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OCCASIONAL PAPERS

OF THE

URRAR^

^UL5 1978
CALIFORNIA ACADEMY OF SCIENCES

, AB: Mass,

No. 129, 1-73 pages, 4 text figures, 18 plates, 1 table

June 22, 1978

Age and Stratigraphic Significance for Lyellian Correlation
of the Fauna of the Vigo Formation, Luzon, Philippines

W. p. Popenoe

Department of Geology. University of California,
Los Angeles. California 90024

and
R. M. Kleinpell

Museum of Paleontology . University of California,
Berkeley. California 94720

^o^DE/^/u

WoED\^''^

SAN FRANCISCO

PUBLISHED BY THE ACADEMY

COMMITTEE ON PUBLICATIONS

Laurence C. Binford. Chairman
Tomio Iwamoto. Editor

Paul H. Arnaud. Jr.

William N. Eschmeyer

George E. Lindsay

The California Academy of Sciences

Golden Gate Park

San Francisco, California 941 18

PRINTED IN THE UNITED STATES OF AMERICA
BY ALLEN PRESS, INC.. LAWRENCE. KANSAS

DEDICATION

This paper is dedicated to the memory of Frank E. Merchant, paleontologist from 1939
to 1941 for the Philippine Bureau of Mines and the Philippine National Development
Company, in association with the present authors. With our advice and encouragement,
he planned to undertake the study and description of the rich and beautifully preserved,
but little known Philippine later Tertiary faunas. In furtherance of this work, he had
been awarded a scholarship at the California Institute of Technology and was on the
point of returning to America to begin his studies when World War II broke out. He
immediately joined the American Army in Cebu, was captured and interned in a military
prison, and died a few weeks afterward of dysentery, pneumonia, and brutal treatment.

With his death, the science of paleontology lost a most promising neophyte, his country
a scholar and patriot, and his associates a fine and valued friend.

TABLE OF CONTENTS

I. Abstract vi

II. Introduction 1

III. Stratigraphy and Paleontology: An Historical Review 3

A. Evidence and Criteria for the Previous Recognition of Miocene on the
Bondoc Peninsula 3

1 . The Stratigraphic Geology 3

2. The Mollusks 4

3. The Foraminifers 6

4. The Algae 8

B. Relevant Later Studies in the Cenozoic of the East Indian Archipelago ... 8

1 . General 8

2. The Mollusks 9

3. The Eoraminifera 10

4. Philippine Stratigraphy and Correlation

IV. Age and Correlation of the Vigo Group, Bondoc Peninsula

A. On the Basis of Eoraminifera and Biostratigraphic Superposition

1 . Stratigraphy

(a) Malumbang Formation

(b) Canguinsa Sandstone 18

2. Biostratigraphy of the Eoraminifera 20

B. On the Basis of the Mollusks 21

1 . The Fauna 21

2. Rates of Evolution 26

V. Acknowledgments 28

VI. References Cited 28

VII. Appendix A: Notes 33

VIIL Appendix B: Register of CIT Fossil Localities 35

IX. Plates 37

Abstract

Popenoe, W. P., and R. M. Kleinpell. Age and stratigraphic significance for Lyellian correlation of the fauna of the
Vigo Formation, Luzon, Philippines. Occasional Papers of the California Academy of Sciences, no. 129, 73 pages,
4 text-figs., 18 plates, 1 table, 1978. — Roy E. Dickerson, in two papers published in 1921, theorized that tropical
Tertiary molluscan faunas evolved much slower than did faunas of temperate regions and that, hence, the percentage
of Recent species in later Tertiary tropical faunas is higher than in contemporaneous faunas from temperate regions.
This theory, derived from analysis of a tropical Philippine fauna of inferred Miocene age, has been frequently cited
but never critically evaluated.

Studies of Philippine and Indonesian Tertiary molluscan and foraminiferal faunas collected since Dickerson's time
and accurately placed stratigraphically indicate that the Philippine molluscan faunas that Dickerson believed to be
of Miocene age are more probably later Pliocene or possibly Pleistocene in age, with a percentage of extinct species
differing not very greatly from the percentages established by Lyell and Deshayes for contemporary faunas of
Europe. The theory that tropical molluscan faunas evolve at a markedly different rate from those of temperate
regions is therefore without foundation and is probably erroneous.

INTRODUCTION

In 1921 the late Roy E. Dickerson wrote two
papers that have had a marked influence upon
subsequent writing in the field of Cenozoic cor-
relation by fossils and the field of organic evo-
lution as a whole. These papers were devoted
to the fauna of the Neogene Vigo Group. Phil-
ippines, and its bearing on the evolution of ma-
rine molluscan faunas (Dickerson 1921a. 1921b).

Dickerson was at that time Honorary Curator
in the Department of Paleontology at the Cali-
fornia Academy of Sciences in San Francisco.
California. It was a period of active and wide-
spread geological exploration for petroleum. In
the Philippines, because of known surface seep-
ages and suitable structural and stratigraphic
conditions (see Pratt and Smith 1913). the Bon-
doc Peninsula of southeastern Luzon had been
receiving more than ordinary exploratory atten-
tion, especially by the Richmond Petroleum
Company, a subsidiary of the Standard Oil Com-
pany of California (see Moody 1922). By 1921.
Dickerson had been able to collect, study, and
publish upon a considerable fauna of fossil mol-
lusks collected from the Canguinsa Formation
and Vigo Group from the south part of this Bon-
doc Peninsula. His record of these data and their
significance first appeared in January 1921 in the
Philippine Journal of Science (Dickerson 1921a)
and. again, with very slight modification, the
paper appeared in July of the same year in the
Proceedings of the California Academy of Sci-
ences (Dickerson 1921b).

In the first of these two papers, Dickerson
(1921a) questioned "the time rate of evolution
of Tertiary molluscan faunas" and followed with
a brief description of the geologic history of his
collection area. He then listed the faunas from
six localities within the upper part of the Vigo
Group. Of the 128 forms which he tabulated in
a "partial list of species from the Vigo Group."
Dickerson noted that "there are 98 forms that
are specifically determined and of these 74 or
75.5 per cent are living species, an astonishing
number when the geologic history of the region
yielding these forms is considered. In addition,
the extinct forms are practically all common to
the upper Miocene of Java, according to K.
Martin." (Ibid.: 10-12)

In pursuit of the age of the Vigo Group, Dick-
erson (1921a: 12-16) gave evidence from earlier
collections of fossil mollusks from elsewhere in
the Philippines and from Java. He further added

stratigraphic evidence from earlier recordings of
larger foraminifers. principally cycloclypeids
and lepidocyclinids, and of the algal reef-lime-
stone-builder. Lithothamnion ramosissimum
Reuss. These data led him to the first of his two
most significant conclusions (ibid.: 16): "From
all the evidence Canguinsa and Upper Vigo beds
may be assigned to some stage of the Miocene,
and the evidence of LepidocycUna indicates a
still greater age, the Oligocene."

With the age of the mollusk-bearing strata
thus determined. Dickerson then discussed the
"importance of guide fossils," "factors pro-
moting evolution of pelecypods and gastro-
pods," "comparison of life conditions during
Vigo-Miocene time with those of Recent time,"
and "crowding of species and the Recent fauna
of the Philippines" (ibid.: 16-20). A summary
paragraph in which is embodied the second of
his major conclusions followed:

The tentative conclusion of the writer is that in the study
of Tertiary faunas of the Tropics a different percentage
scale must be used. For the later Tertiary, Miocene, Pli-
ocene, and Pleistocene the percentages which apply in the
temperate regions to the Pliocene are roughly adaptable to
the Miocene: similarly, the percentages which apply in the
temperate regions to the Pleistocene are apparently those
of the Pliocene of the Tropics. This apparent lack of faunal
differentiation during the Tertiary in the Tropics is due to
uniformity of temperature, salinity, food, and other life es-
sentials. From another viewpoint the rate of evolution of
gastropods and pelecypods in the Tropics during the Ter-
tiary was far less than during this same time in the more
rigorous environs in the temperate zones. The tropical or
subtropical faunas [of the Eocene] of the Pacific Coast of
North America exhibit but slight differences compared to
the faunas of Miocene and Pliocene age of this same region,
and the writer ascribes this to the uniformity of life con-
ditions which prevailed during Eocene time. The amount
of faunal change must not be used as a measure of time in
the whole of the Tertiary, but in measuring the tropic and
subtropic faunas differently marked scales are necessary
for the Eocene and the Oligocene than for the Miocene,
the Pliocene, and the Pleistocene. It is particularly note-
worthy that the Japanese paleontologists are now searching
for comparisons with the Pacific Coast of North America
and Australia rather than with Europe. In other words,
many problems of the tropical Orient will be solved only
when conditions on both sides of the Pacific become better
known [Dickerson 1921a; 20-21J

Subsequently. Dickerson (m Smith 1924: 315)
summed up his conclusion more succinctly with
respect to the significance of the Vigo fauna:

As noted above, the percentage of Recent species is re-
markably high and. from a detailed study of the subject, I
conclude that the evolution of marine molluscan faunas in
the Tropics is far slower than in Temperate Zones ....

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Text - Figure I. Index map of
Philippine Islands, showing
approximate location of im-
portant Neogene sections

I Cagayan Valley, Luzon

2. Bondoc Peninsula

3 Island of Cebu

4 Southwestern Panay
5, Island of Mindanao

On this account the same "yardstick" in the Tertiary geo-
logic time scale cannot be applied in both tropical and tem-
perate regions.

Since Dickerson's time, several papers de-
voted to various aspects of the Philippine Ter-
tiary have appeared (see References Cited). In
many of these, conclusions as to the age and
correlation of the Canguinsa Formation and Vi-
go Group have not agreed with Dickerson's
Miocene age assignment (e.g.. Corby et al. 1951;
Irving 1952; Cloud 1956). yet. few have focused

on the basis for Dickerson's age assignment of
the Vigo fauna or considered alternative corre-
lations. Of greater interest and significance,
however, is the wide extent to which the second
and more far reaching of Dickerson's conclu-
sions has been circulated and tacitly assumed to
have been demonstrated; this concerns a differ-
ential in so-called "rates of evolution"" in Tropic
and Temperate zones and the consequent sup-
posed irrelevancy of Lyellian principle to in-
terregional Tertiary correlation. As an example.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

the reader need go no further afield than a pas-
sage from what in all probability is as sound and
as comprehensive a textbook in stratigraphic
geology as any of the few that are currently
available. In summarizing the origin of the terms
currently employed to designate the series sub-
divisions of the Cenozoic, Dunbar and Rodgers
(1958: 282) note that "Lyell's subdivision of the
Cenozoic into Eocene. Miocene and Pliocene
Series was based primarily on the percentage of
still living species in the several faunas
[although] from the first, he used guide fossils
as well as the percentage of recent species in
recognizing these main subdivisions of the Cen-
ozoic."

In a second paragraph they added:

As study of the faunas of these and other areas pro-
gressed, and the gaps between the Eocene, Miocene, and
Pliocene Series were in part filled by adding the Pleisto-
cene, Oligocene, and Paleocene Series to the sequence, the
characteristic proportions of living species cited by Lyell
were modified from time to time and gradually this basis of
classification and correlation lost its significance, yet the
names have stuck. One of the most searching criticisms of
the method is that of Dickerson ( 1921) who found that fau-
nal changes and extinction during the Cenozoic Era have
been more rapid in the Temperate Zone than in the Tropics,
so that percentages worked out in western Europe are not
usable in lower latitudes. [Dunbar and Rodgers. I9.'^8: 282]

Finally, since this paper was submitted for
publication, Shuto (1975: 296) has written:
"Bondoc Peninsula: The Canguinsa formation
seems to range, at least, from Preangerian to
Miocene/Pliocene transition as suggested by the
molluscan assemblages from Loc. 2. 3. 4, and
5 of Dickerson (1921)."

During the years 1939-1941. we had occasion
to study Tertiary fossils, including foraminifera
and mollusks, from the Bondoc Peninsula. Lu-
zon. The senior author also collected smaller
foraminifers and mollusks from localities that
were reported by Dickerson. In comparing these
fossils from Dickerson's original localities with
those from other areas then being collected by
the Philippine Petroleum Survey, it became ap-
parent that Dickerson's conclusions as to the
age of the Canguinsa and upper Vigo mollusks
were too theoretical to accommodate the evi-
dence available. Evidence from mollusks and
larger foraminifers. and evidence from the su-
perpositional relationships of all three kinds of
fossils in the Bondoc Peninsula and elsewhere
did not support his conclusions. A further com-
parison with the faunas of the Malay Archipel-

ago only served to emphasize these discrepan-
cies in correlation. If Dickerson's Miocene age
assignment of the Vigo-Group mollusks was er-
roneous, his major conclusion concerning rates
of evolution was automatically affected, and es-
pecially so his conclusion concerning a sup-
posed invalidity of the principle of Lyellian cor-
relation.

It is our aim to here focus upon those facets
of the paleontological data that bear upon Dick-
erson's major conclusions and to critically eval-
uate the basis for those conclusions, especially
in light of the additional evidence available.
Hopefully, through such a synthesis, clarifica-
tion of the significance of these data may be
made, not only for the geology, stratigraphy,
and paleontology of the Bondoc Peninsula Ter-
tiary, but also for the principles of Lyellian Ter-
tiary correlation by fossils and for those of or-
ganic evolution as a whole.

We begin with the data and criteria which led
Dickerson to conclude that his 98 specifically
identified fossil mollusks from the Canguinsa
Formation and Vigo Group were of Miocene
age.

STRATIGRAPHY AND PALEONTOLOGY:
AN HISTORICAL REVIEW

Evidence and Criteria for the Previous
Recognition of Miocene on the Bondoc
Peninsula. Southern Luzon

The Stratigraphic Geology. — The marine sed-
imentary strata exposed in the southern half of
the Bondoc Peninsula consist of the lower se-
quence, the Vigo Group, and an upper, the Mal-
umbang Formation, together with some still
higher marine terraces. In general. Dickerson
followed Pratt and Smith (1913) who described
the stratigraphic sequence in detail.

On the peninsula proper the base of the Vigo
is not exposed, its lowermost outcropping beds
are those seen about mid-peninsula in the core
of a close, principally southward plunging, an-
ticlinorium (see Corby et al. 1951: 282. and pi.
26: Irving 1952: 466; Irving 1953: Section 11). In
Dickerson's summary (1921a: 3):

The oldest rocks here recognized consist of shales and
sandstones from 3.000 to 4,000 feet in thickness, the Vigo
group and its uppermost member, the Canguinsa formation.
The strata exposed in the vicinity of Vigo River are steeply
dipping, black, organic shales, subordinate sandstones, and
minor lignitic strata which are unconformably overlain by
the Malumbang formation.

The Malumbang formation consisting of coralline lime-

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

stone and associated marls varies in thickness from small
residuals to 1.000 feet. In a few places . . . marine terraces
truncate the Malumbang strata. These terraces are in places
thickly mantled with coralline limestone of Pleistocene age.
Some . . . may represent high Pleistocene terraces. . . .
These horizons exhibit the same essential conditions in
northwestern Leyte and are beautifully exemplified in the
vicinity of Toledo, Cebu. as well.

After briefly comparing some strata in Min-
danao with those of the Vigo, Dickerson ( 1921a:
3) added: "We are not dealing with local con-
ditions but with general ones which existed over
the site of these islands. . . . Conditions of de-
position during Malumbang and Pleistocene time
resembled those existing today in the vicinity of
the Bondoc Peninsula, and essentially the same
mollusca occur in the coral reef facies of all
three. The deposition during Vigo time was in
marked contrast with these later times, in that
the contributing land masses consisted largely
of diorites. schists, and serpentines or perido-
tites from which they were probably derived."
He concludes (ibid.: 4) that "the sediments were
deposited in the moderately deep waters of an
inland sea with high mountainous islands to the
east. The total time represented since the begin-
ning of the Vigo is evidently long, and on these
grounds as well as faunal, the Vigo group ap-
pears to be as old as the Miocene, and the Mal-
umbang probably represents at least a portion
of the Pliocene."

Dickerson based his paper on collections from
strata that Pratt and Smith referred to the Can-
guinsa Formation and Vigo Group. He believed
that the six fossil mollusk collections were
"from strata which are . . . unconformably be-
low the Malumbang formation." and that "there
are but few places in these islands where good
collections are obtained from localities with sat-
isfactory stratigraphy" (ibid.: 4). Dickerson
(1921a: 4-9) described the six localities and list-
ed the species associated with each, emphasiz-
ing the stratigraphic position in every case in-
sofar as was possible.

Locality 2x [was] on the northeast bank of Bahay River
in a 50-foot cliff of yellow sandstone and bluish clayey
sandstone disturbed by minor faulting. . . . The Malum-
bang limestone is found in the hill 100 yards to the northeast
and from the the general relations in the field it is clearly
unconformable upon the underlying Canguinsa formation.

Locality 3x [was also from the Bahay River but 200 me-
ters upstream from locality 2x and in strata that are] nearly
vertical ... on the southwest bank of stream in a stiff dark
gray shale.

Locality 4x. [again from the Bahay River, but] 320 me-

ters east of the mouth of Apad Creek in road cut 60 feet
above the river in yellow sandstone, about 50 feet strati-
graphically above the . . . lignitic strata of locality 5.

Locality 5 (was also from the Bahay River but] 300 me-
ters east of the mouth of Apad Creek in lignitic gray sand-
stone which was deposited in brackish water.

Locality 9x [was] on Dumalog Creek ... in uppermost
Vigo just conformably below Canguinsa sandstone in black
shale.

Locality llx [was] on west bank of Sapa Tubigbinukot
400 yards upstream from Sapa Yaknes: in soft, yellow
sandstone of Canguinsa age. . . . The strata at this point
dip west about 20" while the overlying Malumbang, a few
hundred feet west, has a gentle dip of 2 to 3". At other
places in this vicinity a notable unconformity separates
these two formations.

The Mo////,vA.s.— Dickerson (1921a: 10-12) list-
ed the species of mollusks collected at his six
localities and noted the percentage of living spe-
cies represented in the fauna. Fourteen of these
were also recorded by Martin (1879-1880) from
the upper Miocene of Java — most were consid-
ered characteristic of that horizon. Only one
other species from Java, Vicarya callosa Jen-
kins, recorded by Martin, was missing from
Dickerson's Bondoc Peninsula localities. But
Martin (1896), in a subsequent paper, recorded
it from apparently the same horizon in the Ca-
gayan Valley of northern Luzon. Two of Mar-
tin's collections were from "Minanga," one
from "4 miles above Minanga," two presumably
from nearby, and the other four from localities
even more difficult to relate geographically, as
well as stratigraphically, to the others. Dicker-
son (1921a: 13-14) listed the species from nine
of Martin's Cagayan Valley localities (these ap-
pear to have been the collecting localities of
Semper). Two of these nine localities yielded
Vkarya callosa: one (locality 8) yielded only
this species, the other (locality 2 from "Minan-
ga; right bank of Ilaroen") yielded this species
in association with seven others, none of which,
however, appear in Dickerson's list from the
Bondoc Peninsula. Among the seven, however,
four (Tcrcbra jcnkinsi Martin. Tercbra handon-
gensis, Murex grooti Jenkins, and Rostellaria
javana Martin) in addition to Vicarya callosa are
noted as having their "occurrence ... in the
Tertiary of other parts of the Indian Archipela-
go" as Miocene (ibid.: 14). A passage from Mar-
tin's discussion of these mollusks from the Ca-
gayan Valley was included by Dickerson (1921a:
13):

Now, in reviewing Semper's collection, I was at once
struck with Vicarva callosa Jenkins, which is known from

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

Java and is described in detail below; and this induced me
to make a closer comparison between the fossils of the
Philippines and those of the Indian Archipelago, whereby
it at once became apparent that a whole series of species,
especially of the Javanese Tertiary is common to both re-
gions. Thus far. indeed. 1 have been unable to make a com-
plete study of Semper's collection, and for the time being
it has little further interest, because statements as to strati-
graphical position are entirely lacking and the equivalent
deposits of neighboring regions are still very insufficiently
known. After completion of my monograph on the fossils
of Java, however. I hope to undertake a more thorough
study of the Philippine fossils, and to supplement this pre-
liminary communication.

From these data, the reader may gather that
Vicarya callosa may be widespread and of more
than ordinary significance in the East Indian
Archipelago as a whole, including the Philip-
pines, and that other species, too. appear to be
common to these two regions. In short. Dick-
erson suggests that at least some strata of Mio-
cene age were probably present at some un-
specified stratigraphic horizon in the Cagayan
Valley (which is more than 200 miles (322 km)
north of the Bondoc Peninsula), that the strati-
graphic ranges of species, at least in Java, might
be stated with more assurance following com-
pletion of Martin's monograph on the Javanese
fossils, that Java and the Bondoc Peninsula
shared several molluscan species in common,
that Java and the Cagayan Valley shared several
other species in common, and that of these sev-
eral species, two (viz., Natica mamilla Lamarck
and Conns loroisii Kiener) occurred both in the
upper Vigo-Canguinsa sequence of the Bondoc
Peninsula and at some stratigraphically unspec-
ified horizon in the Cagayan Valley, none of
which, however, carried Vicarya callosa.

Dickerson (1921a: 14) concluded his evalua-
tion of the molluscan faunas stating:

The fossils in Martin's list come from nine different lo-
calities and the largest number of species from any one
locality is ten. According to Martin, the strata in the vicin-
ity of Minanga belong essentially to the same horizon, and

he says:

Judging from these facts, the strata of Minanga are to
be classed with the upper Miocene bed which exists in
Java in the locality denoted by Junghuhn by O and at
Selatajan on the Tjilongan.

As was indicated above, many of the fossils from the
Bondoc Peninsula are common to this locality O in Java,
and the equivalence of the Upper Vigo beds with these
Javan beds is evident. Upon the basis of Martin's work,
the age of the Vigo beds is upper Miocene.

In a subsequent section. "Importance of guide

fossils," Dickerson added another paragraph
having direct bearing on the age of his mollusks.

As will be seen from a study of the fauna cited above, most
of the forms which are extinct were originally described
from a correlative horizon in Java. Of these, the writer is
inclined to think that Cerithium jenkinsi . C. herklotsi. C.
handongensis . Mitru javana. M. jenkinsi. M. junghtihni .
M. bucciniformis . Tunis coronifer. Terebra bicinctu. Tcr-
cbru javana . Vicarya callosa . and Vcrmclus javanus will
probably prove reliable guides among the mollusca. (Ibid.:
161

The two cones and the columbellid previously
listed from Martin's Javanese localities were
omitted here; otherwise the lists are the same.
Concerning these twelve species. Dickerson
(1921a: 16) notes that "All of these species are
representatives of highly organized genera and
their extinction during the post-Miocene time
was probably due to their inability to obtain life
conditions suited to their highly specialized
needs."

Before leaving this review of the direct mol-
luscan evidence for the Miocene age of the up-
per Vigo and Canguinsa molluscan fauna, it
seems appropriate to refer again to Dickerson's
(/// Smith 1924) subsequent discussion of the
same Vigo and Canguinsa formations and their
mollusks. In Table 24 of that work. Dickerson
listed 1 18 species that he previously (1921) listed
from the Bondoc Peninsula Vigo Group, and 1 19
forms in total. He again stated that "about 75
per cent of the specifically determined forms are
living species, an astonishing percentage when
the geologic history of the region yielding these
forms is considered" (ibid.: 315). Conspicuous,
however, in this 1924 list, is the presence of Vi-
carya callosa. previously absent from the Vigo
list in his 1921 paper. No Bondoc Peninsula lo-
cality for this species was given, though, as in
the earlier work, he listed it from other areas in
the Philippines (Batan Island. Mindanao, Cebu
and "from sandstones, lignites and shaley lime-
stones which dip at an angle of 35° beneath the
coralline limestone of Mount Mirador ... six
kilometers west of Baguio northern Luzon"
(ibid.: 326-327)). In discussing the age of the
Batan Island coal deposits. Dickerson noted that
"in the gray shale overlying the East Batan coal
seam in the Perseverancia claim, very excellent
specimens of Vicarya callosa Jenkins and nu-
merous species of Corbnla were obtained by F.
A. Dalburg (Bureau of Science locality No. 7)"
(ibid.: 319). On the following page he stated:

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

... it is my opinion that this Batan coal is essentially of
the same age as is the coal of Cebu and of tunnel 14 of
Sibuguey Peninsula. Mindanao. At the latter place. Dalburg
collected splendid specimens of Vicarya callosa Jenkins
from the coal seams and shales (Plate 9, fig. I). Vicarya
callosa is associated with the coal seams of Cebu and
seems to be a form which flourished in brackish water.
Whether or not this form is very limited in geologic range
is probably open to question, as those forms which have
a great geographic distribution frequently have a consid-
erable stratigraphic range as well. It is probably limited to
the Vigo group at least; that is. to about 1,000 meters of
sedimentary beds, as it never has been reported from the
Malumbang formation.

Douville places locality 272 in his II. 2, the Lepidocyclina
limestone. The Bureau of Science possesses an excellent
collection of gastropods and pelecypods from this place
collected by Smith, among which the following forms have
been identified. [Dickerson />i Smith 1924: 320]

and he then lists the following from "Locality
F272 (Cebu)": Bullaria ampulla (Linnaeus),
Conns sp., Cerithium (Campanile) sp., Ceri-
thium sp., Cerithium jenkinsi K. Martin, Ceri-
thium herklotsi K. Martin, Cypraea sp.. Fiisinus
sp.. Natica sp..TurbinellaJunghulini K. Martin.
Trochus sp.. Turbo sp. a. Seraphs sp., Vicarya
callosa Jenkins, Voluta innexa Reeve, Chione
lacerata Hanley. Lucina sp., Pecten cf. lenti-
ginosus Reeve. Pecten leopardus Reeve, Pli-
catula imhricata Menke. Concerning this as-
semblage he adds, "A brief comparison of these
forms with collections from the Vigo group of
the Bondoc Peninsula clearly demonstrates es-
sential faunal unity" (ibid.). Of the nine forms
specifically identified in this assemblage of twen-
ty forms, three are in common with the earlier
(1921) list from the upper Vigo and Canguinsa
of the Bondoc Peninsula; four are in common
with those listed in the preceding table as from
the Vigo Group, the extra species in the latter
instance being Vicarya callosa .

Further discussion of the age and correlative
significance of the upper Vigo and Canguinsa
mollusk fauna from the Bondoc Peninsula is left
for a later page, when the problem is reviewed
in the light of additional data.

The Foraminifers. — The balance of Dicker-
son's direct paleontological evidence for the
Miocene age of the Vigo-Canguinsa fauna of the
Bondoc Peninsula consists of foraminifera. For
the sake of clarity, the pertinent passages from
Dickerson (1921a: 14-15) are quoted in full.

Martin lists the distinctive foraminifera, Cycloclypcus
communis Martin from his (and Junghuhn"s) localities K,
L, O, and P.; Orhitoidcs f>igantca Martin is from locality

O; and O. radiata Martin is from locality K. The localities
all represent about the same horizon in Java and it is im-
portant to note these forms here, as they are regarded as
excellent horizon determiners.

Dr. W. D. Smith [footnote reference here to Pratt and
Smith 1913: 330], on the strength of the occurrence of Cv-
cloclypcus communis K. Martin and Lepidocyclina richth-
ofcni Smith, refers the Canguinsa sandstone to the middle
or lower Miocene. His exact statement is as follows:

.... The limestone from Mount Morabi . . . contains
Cycloclypcus communis K. Martin, which represents the
middle Miocene, and large lepidocyclinas some of which
are 45 millimeters in diameter and ."i millimeters broad in
the thickened central portion. Lepidocyclina richthofeni
Smith was identified among these. This species has been
referred by Douville to the lower Miocene.

No definite age determination can be made from the
fossils in the Canguinsa sandstone proper. The fossils in
the included limestone, however, are well known and
have been used in correlation by various authorities.
From their presence it is concluded that the Canguinsa
sandstone should be placed in the middle Miocene, ex-
tending perhaps into the lower Miocene.

In a recent publication. Prof. H. Yabe [footnote refer-
ence here to Yabe 1919: 40| gives a full discussion of cor-
relation of these equivalent beds in Cebu, and Smith's and
Douville's correlation tables are quoted. It is noteworthy
that the beds under discussion are classified by Douville as
Aquitanian. All who have studied the large foraminifers
from the Philippine Islands agree that one of the charac-
teristic genera is Lepidocyclina . Cushman [footnote refer-
ence here to Cushman 1918: I15[ in a recent paper makes
the following significant statement:

Because, in general. Orbitoides with some modifica-
tion to be noted in a future paper, is Cretaceous, Orttio-
phrugmina Eocene and Lepidocyclina Oligocene, much
importance is attached to these organisms in the inves-
tigation of problems of geologic correlation.

For the purpose of placing Dickerson' s crite-
ria for age and correlation in their relevant con-
text here, it needs to be noted that Cycloclypcus
communis, sensu lato, ranges geologically from
Oligocene to Recent (see Corby et al. 1951: pi.
31; and Colem Ladd and Hoffmeister 1945: 280,
for a distinction between the "C. communis'^ of
Douville and that of Martin; and see also Cole,
op. cit.: 273. 279). and that the "limestone from
Mount Morabi" referred to by Smith is at the
very least stratigraphically 1.000 ft (305 m) (and
probably more than 2,000 ft (610 m)) below the
base of the Canguinsa Formation as used by
Pratt and Smith (1913) and by Dickerson
(1921a).

Dickerson (/// Smith 1924: 309-322) made fur-
ther reference to the foraminiferal evidence for
a Miocene age for this fauna under the subhead-
ing "Lepidocyclina limestone facies of the Vigo
group." He discussed, under this subheading.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

Douville's classification of foraminiferal samples
collected by W. D. Smith from Batan Island
(Caracaran. locality 2. and the soft sandy yel-
lowish limestone of Gaba Bay. locality 8) and
from the islands of Cebu (Sibul Gulch, old Al-
paco Mine, locality 273; limestone of Guila-Gui-
la, locality 278; limestones of the Barrio of Mes-
aba, locality 272; limestones of the valley of
Cumajumayan. locality 28; the Compostella
Mine, locality 289; along the road from Toledo
to Cebu, on the edge of the Minanga River, lo-
cality 277, near camp 1 ; and the "very soft white
limestone which runs along the cordillera central
of Cebu Island, Valley of Cotabato," locality
279). Douville had concluded that these large
foraminifers ranged in age from Oligocene Stam-
pian to Miocene Burdigalian. Following a dis-
cussion of the stratigraphic relationships of
these larger foraminifers to the associated mol-
lusks, Dickerson (op. cit.: 321) returned to the
large Foraminifera which "Smith reported . . .
from Bondoc Peninsula from beds of Canguinsa
age." Here Dickerson quoted part of an earlier
(1921) passage referring to "the limestone from
Mount Morabi," but without W. D. Smith's ear-
lier qualification as to the age of "the fossils in
the Canguinsa sandstone proper." Concerning
these. Smith had clearly stated. "No definite age
determinations can be made from them." Dick-
erson then added, in this (1924) paper.

This Lepidocyclina fauna occurs in the upper portion of
the Vigo group, the Canguinsa formation |sic|. This for-
mation in the same region has yielded a large part of the
mollusks reported above, and it is clear that the vertical
range of the large representatives of the genus Lepidocy-
clina is much greater than Douville suspected.

H. Yabe (footnote reference here to Yabe 1918: 2). in a
recent publication, recognizes this possibility and he re-
views the case as follows:

L. Rutten studied foraminiferal rocks from southern
and eastern parts of Borneo and found it necessary to
modify somewhat H. Douville's correlation of the Ter-
tiary rocks, because Lepidocyclina appeared to have a
more extended vertical range than was believed by Dou-
ville. Thus, the oldest Miocene and Oligocene deposits,
according to Rutten. are characterized by Lepidocycli-
nas of larger and smaller sizes, while the smaller ones
alone are found together with Miogypsina in all parts of
Miocene deposits except the lowest division.

Rutten (footnote reference here to Rutten 191 1-1914:
287] presents a table in his paper which is copied by
Yabe. Yabe [footnote reference here to "659,"' appar-
ently Yabe 1919: 37-51] in another and later paper upon
the Lepidocyclina limestone from Cebu. recognized Lep-
idocyclina (Nephrolepidinu) angulosa Provale associated
with Lepidocyclina monstrosa Yabe, Lepidocyclina for-
mosa Schlumberger. and several other Foraminifera. It

is evident from this assemblage that the section Ne-
phrolepidina is not restricted to the uppermost horizon,
as Douville thought.

Briefly, in conclusion, then, the Lepidocyclina lime-
stone is equivalent to the shales and sandstone of the
Vigo group and the molluscan faunas of the latter beds
are equivalent to the large-sized Lepidocyclina fauna of
Cebu. In other words, the limestones, shale, sandstones,
and coal are different depositional facies within the same
group, the Vigo of probable middle and upper Miocene
age.

Again, the systematics here involved could be
clarified to advantage. Clearly, the bearing of
these Lepidocyclina-carrying limestone beds
upon the age of the upper Vigo and Canguinsa
mollusk fauna of the Bondoc Peninsula is one of
superpositional relationships. Needless to say,
the islands of Batan, Cebu and Mindanao are
many miles removed from each other as well as
from the Bondoc Peninsula and, similarly, the
Cagayan Valley and the Baguio area of northern
Luzon are distantly removed. Even Mount Mor-
abi is about five miles (8 km) from the Canguinsa
mollusk-bearing outcrops. Pratt and Smith rec-
ognized an unconformity at the base of the Can-
guinsa which intervenes stratigraphically be-
tween the orbitoidal limestones in reference and
most of the mollusk-bearing Canguinsa strata.
However. Dickerson clearly disagrees with Pratt
and Smith regarding the presence of this uncon-
formity. In his 1921 paper the particulars are
vague: "The writer's view concerning the stra-
tigraphy of the region under discussion differs
in this regard from that of Pratt and Smith, but
a full exposition of this important point cannot
be given here" (Dickerson 1921a: 3. footnote).
But in his subsequent paper (1924). Dickerson's
views are made clear.

I am not in agreement with Pratt and Smith concerning
the stratigraphic relations of the Malumbang. Canguinsa,
and Vigo in their type localities. Bondoc Peninsula. I be-
lieve that a great unconformity exists between the Mal-
umbang and the underlying Vigo group. I failed to recog-
nize an unconformity between the Canguinsa formation and
the Vigo shale, although the areas cited by Pratt and Smith
were critically examined. The relations that appear at these
places are best explained by faulting. On this account the
term "Vigo" is widened to include the Canguinsa forma-
tion as its upper sandstone facies. thus raising the term
Vigo to a group rank. [Dickerson in Smith 1924: 313,
footnote]

Subsequent field studies by the present au-
thors and the field parties of the Philippine
Petroleum Survey and the Philippine Oil De-
velopment Company have indicated the

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

controversial unconformity to be local, with
elsewhere a local sandstone and fine sandy con-
glomerate occurring gradationally between the
underlying dark claystone of the Vigo and the
lowermost beds of the Canguinsa. sensn stricto.
At one locality a single small outcrop of volcanic
agglomerate occurs at the horizon of Pratt and
Smith's "unconformity" at the base of the Can-
guinsa. sensii stricto. Yet. whether a mere dia-
stem is reflected, or a hiatus of greater magni-
tude indicated, is not clear from the physical
evidence. In any event, the notable geographic
distance between the respective fossil localities
and the intervening stratigraphic interval of at
least 305 m. and probably more, both remain.

Thus, the residue of evidence for the contem-
poraneity of the moUusks and larger foraminifers
stressed by Dickerson is of two kinds: one. in-
direct evidence involving species from widely
separated islands that are interpreted to be cor-
relative, although many of the forms involved
turn out to be long-ranging species and the
diagnostic species were absent in the critical lo-
calities; the other is direct evidence involving
occurrences within a single formation, the Vigo,
raised to group rank by Dickerson and suppos-
edly "from 3.000 to 4.000 feet in thickness"
(Dickerson 1921a: 3), though not at all clearly at
the same stratigraphic horizons within that
group or formation.

The Algae. — The remaining paleontologic evi-
dence for the Miocene age of the upper Vigo and
the Canguinsa mollusk fauna of the Bondoc Pen-
insula is clearly indirect, though again super-
positional since it involves the presence of Lith-
othamnion ramosissimum Reuss in the lower
limestone of the overlying Malumbang Forma-
tion. But from Dickerson's discussion, it is ap-
parent that even he came to regard the strati-
graphic significance of this fossil as equivocal.
Concerning this, Dickerson (1921a: 15-16) first
quoted Pratt and Smith (1913: 327). then Yabe
(1918: 14), in the following passages:

Pratt and Smith state the case as follows:

The most conclusive evidence as to the age of the
Malumbang series is found in the Lower limestone,
which, on the basis of the fossil Lithothamnion ramosis-
simum Reuss . . . may be assigned to the Miocene. The
upper beds in the series are apparently as voung as the
upper Miocene or Pliocene. The formation is similar to
the "etage marneux" which Verbeek assigns to the mid-
dle stage of the upper Tertiary for Java.

Concerning the range of this species. Prof. H. Yabe...
notes the following:

This reef building organism is very often cited from
the limestone of the Oligocene and Miocene ages of the
Indo- Pacific region, its occurrence being known from Ja-
pan, the Philippines. Borneo, Timor. Amboina, New
Guinea and adjacent islands. New Hebrides, Victoria,
the Christmas Is. etc.

In Japan it is found not only in Lepidocyclina and
Miogypsina-limestone and similar and equivalent beds of
Formosa, Botel-tobakee. the Riukiu Islands and the
Ogasawara-Jima, but also in the Lepidocyclina and Mio-
gypsina-limestones of the provinces of Sagami and Kae,
2, the Lithothamnion-limestones of Oyami-Yama and
Megami-yami near Sagau, Province of Lotomi; and 3,
the Lithothamnion-limestone intercalated in an oil-bear-
ing Tertiary complex of Echigo, 4. the Lithothamnion-
limestone of Shiroiwa, Makatsuka-mura, Otsu-gou,
Province of Natigo.

It is evident from these references that this form has
considerable range in the Miocene and probably the Pli-
ocene.

In his subsequent paper. Dickerson (in Smith
1924: 327) quotes Smith in reference to Smith's
work on the Sagada Limestone of Mountain
Province, as recognizing therein "the well-
known Mio-Pliocene marine alga. Lithotham-
nion ramosi.ssimiim Reuss." and Dickerson (op.
cit.: 322. 331. and Table 3) consistently refers to
the Malumbang "Pliocene."

Relevant Later Studies in the Cenozoic
OF the East Indian Archipelago
General. — In the two decades that followed
Dickerson's evaluation of the fauna from the
Vigo Group, much additional information has
come to light concerning the Cenozoic inverte-
brates of the East Indies (including the Philip-
pines) and their stratigraphic distribution
throughout the archipelago. More than one syn-
thesis of these data have appeared during this
interim. Some have emphasized the geologic
history of the region, some its stratigraphic pa-
leontology, and others the economic signifi-
cance of the geology and stratigraphy of the
area.

With these extensive regional studies, more
detailed comparisons are possible between the
Cenozoic of the Philippines and that of the Ma-
lay Archipelago as a whole. The molluscan stud-
ies of Martin and others have been concluded.
The sequence of Tertiary larger foraminifers has
come to form the bases for a biochronologic
classification of the East Indian Tertiary — the
so-called "letter classification" first proposed
by Van der Vlerk and Umbgrove (1927) and later
expanded by Leupold and Van der Vlerk ( 1931).

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

A record of the smaller foraminifers and their
stratigraphic distribution has been added to
some extent. In addition to the Leupold and Van
der Vlerk (1931) summary, a geologic history of
the East Indies (Umbgrove 1938) has paid not-
able attention to the Cenozoic stratigraphic ge-
ology and stratigraphic paleontology. In the
Philippines economic and geologic reports by
Corby et al. (1951) and by Irving (1952. 1953)
have summarized, in reconnaissance fashion,
the distribution of the Cenozoic in much of that
archipelago. Cloud (1956) has placed these East
Indian faunal and formational sequences into re-
lationship with those of the Cenozoic of the Pa-
cific basin as a whole. Within the context of
these syntheses, the Neogene faunas of the
southern Bondoc Peninsula have come into
sharper focus than was possible in Dickerson's
time. These syntheses have particular signifi-
cance in that conclusions drawn as to the age of
the Neogene faunas of the southern Bondoc
Peninsula and as to the so-called rates of evo-
lution of these faunas differ considerably from
those of Dickerson which, nevertheless, have
tended to persist.

We review first these regional syntheses;
then, in the light of these data, we re-examine
the Neogene sequence in the Vigo Group of the
Bondoc Peninsula.

The Mollusks. — Karl Martin's studies of the
East Indian Tertiary mollusks occupied more
than fifty years of his lifetime. Dickerson. in his
comparisons with Martin's upper Miocene mol-
lusks from Java, apparently made all of his de-
terminations from two of Martin's first publica-
tions. "Tertiarschichten auf Java" (1879-1880)
and "Tietliohrungen auf Java" (1883-1887). The
tremendous amount of work that Martin did sub-
sequently on the faunas may have been un-
known to Dickerson. Dickerson seems to have
been unaware of Martin's 1919 work ("Unsere
Palaeozoologische Kenntnis von Java") in
which Martin explains his own extinction-per-
centage scheme for the East Indies Tertiary.
Martin considered his Tjilanang beds, together
with Junghuhn's locality "O" to have 34% Re-
cent species, these constituting the horizon with
which Dickerson correlated his Bondoc Penin-
sula faunas with 75% Recent species. In 1921.
Martin listed the percentages of Recent mollus-
can species in the Tertiary of Java as follows
(Martin 1921; see also Davies 1934: 57; and Po-
penoe in Corby et al. 1951: 253-254):

Pleistocene 86 to 90%

Pliocene 5 1 to 64%
Odeng beds 43%

Tjilanang beds 34%

Njalindung beds 21.6%

Rembang beds 16.9%

West Progo Miocene 6.8%

Upper Eocene & (?)01igocene 0%

As Davies (1934: 57) noted. "Here the steady
increase in the percentage is obvious."

Pointing out that the terms "Eocene." "Mio-
cene," "Pliocene." etc., used in his classifica-
tion could not be held to represent exactly the
same periods of time as the European Tertiary
epochs so named, Martin classified these Javan
molluscan faunas thus:

"Pleistocene" — 80% or more Recent species
"Pliocene" — 50-80% Recent species
"Upper Miocene" — 20-50% Recent species
"Lower Miocene" — 8-20% Recent species
"Eocene" — no Recent species present

So the "West-Progogebirge beds," Rembang
Beds, and Njalindung Beds served as guide for
the "Upper Miocene," and the fauna from the
Sonde Beds, with 150 molluscan species (53%
Recent), furnished guide fauna for the "Pli-
ocene" (see Popenoe in Corby et al. 1951: 253-
254). The Fufa Beds of Seran and Obi, with a
fauna of 158 species of which only 46.8 per cent
were Recent, were also considered "Pliocene"
by Fischer (1927: see also Popenoe in Corby et
al. 1951: 260).

Martin (1919) included lists of important
though less comprehensive publications dealing
with the Tertiary paleontology of the Indo-Pa-
cific region. A list of Martin's major papers on
the subject, along with those of Tesch ( 1920; on
Timor). Fischer ( 1927) and Van der Vlerk ( 193 1 )
is given by Popenoe (in Corby et al. 1951; 263).
Van der Vlerk ( 193 1 ) gives a complete list of all
Cenozoic mollusks reported or described from
the Dutch East Indies up to 1931, with geologic
range, references, a complete bibliography, and
critical notes.

By 1927 Van der Vlerk and Umbgrove had
further subdivided the East Indian Tertiary on
the basis of the stratigraphic ranges of foramin-
ifers. Leupold and Van der Vlerk (1931; 611-
648) summarized the Tertiary history of the East
Indies, employing 8 stages and 16 zones "based
upon vertical distribution of larger foraminif-
era." They grouped these stages and zones into

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No, 129

a "Tentative general subdivision of the Tertiary
of the Dutch East Indies based on the main
stratigraphic features (transgressions, uncon-
formities). . . ."' with corresponding "percent-
ages of still living species of Mollusca" as fol-
lows:

Upper Tertiary

Upper: Stage h.

Zone 2

60%

Zone 1

50%

Stage g

45%
35%

Stage f.

Zone 3

30%

Middle: Stage f.

Zone 2

20%

Zone 1

18%

Stage e.

Zone 5
Zone 4

Lower: Stage e.

Zone 3
Zone 2
Zone 1

Stage d

Lower Tertiary

Upper: Stage c

Middle: Stage b

Stage a.

, Zone 2

Lower: Stage a.

Zone 1

A more recent percentage distribution summa-
rized by Umbgrove (1933) has not notably al-
tered these percentages.

Meanwhile, in the Philippines, the major ad-
ditional contribution to the molluscan paleon-
tology was probably that of Faustino (1926;
1928). He reviewed the disputed Oligocene or
Miocene age of the typical Vigo Shale (ibid.; see
also Corby et al. 1951: 238. 248-249) and fo-
cused attention on the conflicting evidence pre-
sented by the mollusks and the larger foramini-
fers as correlated by Douville (1909). Again the
controversy centered around the Oligocene or
Miocene age of the lowest of these beds and
around the identification and biochronological
significance of a gastropod, Ainpullinopsis , and
of certain aberrantly small ''Niimmiilitt's" (N.
suhniasis) that are associated with Lcp'uiocycli-
na in the lowest of the Batan Island beds from
which the suite of larger foraminifers studied by
Douville were collected (see Douville as quoted
by Dickersonm Smith 1924: 317).

During 1939-1941, field parties of the Philip-
pine Petroleum Survey assembled an extensive
collection of fossil mollusks, principally from

the island of Panay, but also from Cebu and else-
where, and on Luzon from the Bondoc Penin-
sula, the Batan Island area and the Cagayan
Valley. Oldest were Jurassic ammonites from
relatively undisturbed strata on Mindoro (Corby
et al. 1951: 68). but most were of Neogene age.
A partial list of the mollusks from these collec-
tions was presented by Popenoe (in Corby et al.
1951: pis. 36, 37, 44-46) together with their
known geologic ranges in the East Indies and in
the Philippines. The 152 Philippine localities
from which these mollusks were collected were
assigned a geologic age by Popenoe and Mer-
chant in the same publication (ibid.: pi. 38), as
were also the mollusks and the 60 mollusk-bear-
ing Philippine Tertiary localities on record in the
literature prior to 1939 (ibid.: 32-33). Popenoe
(op. cit.: 252-264. and also pi. 47) presented a
preliminary discussion of the molluscan faunas,
their geologic age, and their relationships with
the Tertiary molluscan faunas of the East Indies.
In view of the direct bearing of these Philippine
mollusk collections upon the age and signifi-
cance of the molluscan fauna of the Vigo Group
of the Bondoc Peninsula. Luzon, they are dis-
cussed in detail in the concluding section of this
paper.'

The Foraminifers. — Since Dickerson's (1921a,
1921b) works, the most important clarification
of the age and stratigraphic distribution of Ter-
tiary foraminifers in the East Indies resulted
from the so-called "letter classification" of Van
der Vlerk and Umbgrove (1927). Leupold and
Van der Vlerk (1931) used this letter classifica-
tion to provide the time coordinate for their
summary of the East Indies Tertiary.

A jubilee book in honour of Professor Martin is the right
place for an essay on the Tertiary of the Dutch East Indies,
as it was he who laid the foundations of stratigraphy in that
district.

The basis upon which he founded the subdivisions of the
Tertiary deposits has proved the firmer the more it has been
tested.

He laid down two fundamental principles upon which
further investigations have been built.

In the first place he showed that during the Tertiary an
autochthonous fauna developed in the East Indies and in
the second place he insisted that a subdivision of the Ter-
tiary systems can only be obtained by comparing their fos-
sil contents with the fauna that still exists in these regions
and not with the European Tertiary fossils. It might appear
to be a simple matter to compare fossils with living species,
but when entered upon it is found to be difficult in the
extreme. Thousands of molluscs have passed through the

' See Note i in Appendix A.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

hands of this untiring investigator and only those who have
themselves experienced the endless difficulties that attach
to the determination of fossil material are able to form an
idea of the energy it must have cost to bring this compar-
ative study to a satisfactory conclusion.

As the fauna that flourished in the East Indies was en-
tirely different, it is not possible to apply the names current
for European series with typical faunas to the East Indian
Tertiary epoch.

The investigations of Vredenburg and DeCotter. in Brit-
ish India have rendered it possible to make a rough com-
parison between Java and Europe via Burma and North-
western India (vide: MARTIN. Leidsche Geol. Meded.,
Deel IV, Afl.l), but a detailed correlation is not possible.

The authors have therefore decided to use the subdivi-
sions by letters as proposed by VAN DER VLERK-
UMBGROVE (Wet. Meded. No. 6).

The basis for the subdivision in stages and horizons is
formed by the foraminifera of the strata.

As tabulated on a previous page, the "letter
classification" serves to subdivide the Tertiary
of the East Indies into 8 stages and 16 zones.
The ranges of the 52 diagnostic large foraminifer
genera and species upon which this classifica-
tion is based are tabulated by Leupold and Van
der Vlerk(1931).

Stages a. b, and c. which do not directly con-
cern us. are based primarily upon the ranges of
certain species of Comerina, of '^FasciolitesS^
and of the genera Assilina , Pellatispira , Heter-
ostegina. and Discocyclina: the sequence a-1
through c was considered to range from lower
Ypresian through lower Oligocene by Gerth
(1929). Stage c of southeastern Borneo was
equated with the Sannoisian by Douville. Stage
d, also not directly involved in the problems of
the Bondoc Peninsula Vigo Group fauna, carries
the highest Camerina (three species, notably in-
cluding C. fichteli-intermedia , which is shared
with Stage c only), the reslncled Isolepidina and
Eiilepidina papiiaensis . together with the lowest
Cycloclypcus -dnd Lcpidocyclina (the latter in is-
olepidine and eulepidine forms); Stage d is con-
sidered Stampian in age by Douville and "Upper
Oligocene" by Gerth (1929).

Stage 3. the oldest involved in possible cor-
relations with the Vigo Group of the Bondoc
Peninsula is considered of Aquitanian age by
both Douville and Gerth. of "Lower-Upper
Aquitanian" by Tobler (1918) following Dou-
ville. and as (upper?) "Mio-Oligocene" by Rut-
ten (1911); it carries the highest Eidepidina . scn-
su striito. and "Clausidus pygmaeus ( = Alv. sp.
3 Verb.)." the lowest Nephrolepidina and Tril-
lina howchini . and is further zoned on the basis

of species of Lcpidocyclina , sensu lata , and Spi-
roclypcus . with ^^Tryhliolcpidina .'^ Miogypsina ,
and Alvcolina appearing in its upper two zones.

With Tertiary Stage f. the "letter classifica-
tion" enters unequivocal Miocene. Zonation
within the stage leans heavily upon species of
Lcpidocyclina and Miogypsina of which all re-
maining species make their last stand in Zone f3
which in turn is characterized by the restricted
occurrence of "Trybliolcpidina" nitteni. Diag-
nostically also. ^^ Alvcolina boscii"^ appears in
Zone fl to range upward through the "Pli-
ocene," whereas "A. hontangcnsis^" becomes
extinct at the top of Zone tl.

Finally, it is significant that Stages g and h
(including the two zones, hi and h2) reveal
merely negative evidence in terms of the larger
foraminifers; shown as present throughout, but
all ranging upward from lower beds, are Hcter-
ostegina. Cycloclypcus, and Alveolina. Diagnos-
tic distinctions clearly are based upon different
percentages of living mollusk species (35% and
45%. presumably in higher beds, for Stage g.
50% in Zone hi. 60% in Zone h2). The smaller
foraminifers are still another element in the East
Indian Tertiary faunas that aid in subdividing the
stratal sequences on a biochronological basis
(see Koch 1923. 1925, 1926; Boomgaart and
Vroman 1936; Boomgaart 1949; Caudri 1934;
Tobler 1918; LeRoy 1938a. 1938b, 1939. 1941.
1944. 1948). With the disappearance, at the top
of the "Miocene" (i.e.. top of Tertiary f3). of
the previously dominant lepidocyclines and mio-
gypsines. the inshore shallow-water facias of
East Indies Neogene witnesses an increase and
diversification of mollusks in an expanded
coarsely clastic lithofacies and a flowering and
diversification of benthonic small foraminifers in
the marls and more finely clastic inshore facies
of the "Pliocene" generally. This is perhaps
most conspicuous in the genus Ammonia, or
"/?(>rfl//rt." of which stock "Rotalia'' papillosa
Brady (see LeRoy 1941) is an especially con-
spicuous and widely flourishing newcomer.
Stratigraphically it is not known from the "or-
bitoid"-bearing horizons of Stage f (though the
less ornate ancestral species of the stock do oc-
cur), and even its occurrence in beds of the in-
tervening Stage g is rare and sporadic, doubtful
at best. The distinction between the "orbitoid"-
bearing "Miocene" beds of Stage f. below, and
the "Rotalia" papillosa-bearing beds of Stage
h. above, had been so consistently noted that

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

the term "Rotalia Zone'" had. by the late 1930's.
come into wide usage for the ""PHocene"" in re-
connaissance petroleum exploration from Bor-
neo and Java eastward to New Guinea (see Cor-
by et al. 1951: 288; Kleinpell 1954b: 22; 1958: 4-
5).

As work has progressed throughout the Indo-
Pacific region as a whole, some of the zonal dis-
tinctions embodied in the Tertiary "letter clas-
sification'" have become blurred. Thus, it has
ceased being possible to distinguish on the basis
of the larger foraminifers alone all the five zones
of Stage 3 over a broad area, and similarly Zone
O has tended to blend either upward or down-
ward with the other two zones of Stage f (see
for example Glaessner 1943. 1953. 1959). Thus
Stage 3 today is usually subdivided into a lower
(el-e2-e3) and an upper substage or zone (e4-
e5). although Zone e5 is. in some areas at least,
subdivisible into two zones, as was suggested in
the original Leupold and Van der Vlerk (1931)
chart showing the ranges of Spiroclypeus . S. ti-
doenganensis, S. leupoldi, S. margaritatus,
Miogypsina dehaarti. and "Alvcolina" bontan-
gensis. Zone f2, in terms of large-foraminifer
ranges, hinges upon nothing more distinctive
than a somewhat higher range of Ncphrolcpidina
sKmatrensis . N. s. var. douvHlei. and the mio-
gypsines that lack lateral chambers, in relation
to the not-so-high highest occurrences of Pliole-
pidina. Ncphrolcpidina bornccnsis . N. vcrbccki .
and certain species of microspheric lepidocyc-
lines that are less than 15 mm in diameter.
Nevertheless, locally at least, as in the Philip-
pines (see Corby et al. 1951). small-foraminifer
species apparently serve to distinguish a "mid-
dle f Zone from lower and higher fl and f3
equivalents, respectively. However this may be.
the more commonly accepted "letter classifi-
cation" in modified form is succinctly shown in
the correlation chart for the Cenozoic of the
western and central Pacific by Cloud (1956: pi.
1 ) in which he essentially follows the modifica-
tions of Van der Vlerk (1950; see also Cloud
1956: 557-563 for a general discussion of the
problem).

In the Philippines both the larger and the
smaller foraminifers have received considerable
attention since the earliest geological studies.
Oldest known to date are mid-Cretaceous Or-
bitolina from metamorphics in Cebu (Corby et
al. 1951: 68; see also Arnold and Kleinpell 1951).
Large foraminifers were the first Cenozoic fos-

sils recognized in the Philippines (Richthofen
1862); originally thought to have been nummu-
lites of Eocene age. these large foraminifers
from the Binangonan Peninsula. Laguna de Bay.
Luzon, were subsequently shown by W. D.
Smith ( 1906) to be orbitoids of the genus Lcpi-
docyclina and of post-Eocene age. Abella y Cas-
ariego (1886) recorded "nummulites" from Ce-
bu which, too. subsequently proved to be
Lepidocyclina; and the record of orbitoids and
cycloclypeids by Martin (1896; see also Becker
1901 for the English translation) has already
been mentioned in connection with his recog-
nition of Cenozoic mollusks in the Cagayan Val-
ley and La Union Province. Luzon, and the
Agusan Valley of Mindanao. Subsequently,
Martin (1901) again recorded orbitoids from
southern Luzon, and W. D. Smith's (1906) de-
scription of the orbitoids of Binangonan and of
the Loboo Mountains followed. H. Douville
(1909, 1911) described and correlated orbitoid
samples collected by W. D. Smith on Cebu and
on Batan Island, and a decade later Yabe (1919)
published the first of a series of papers by Jap-
anese investigators on the Philippine species of
Lepidocyclina and their stratigraphic signifi-
cance. Smaller foraminifers from the Philippines
were first recorded by von Drasche ( 1878) in the
report of his reconnaissance of Luzon which in-
cluded a report by Felix Karrer (republished in
1880. in Spanish) on some Tertiary small fora-
minifers collected from the west coast of Zam-
bales Province. Luzon; these Kairer related to
the younger Tertiary smaller foraminifers de-
scribed by Schwager (1866) from Kar Nicobar.
Attention to both the larger and smaller for-
aminifers of the Philippines has been more ex-
tensive since Dickerson's time, though not as
comprehensive as in the Dutch East Indies. Two
of the most significant additions to the knowl-
edge of Philippine larger foraminifers appeared
in papers by Yabe and Hanzawa (1925, 1929);
in the first, faunas collected by Dickerson from
Cebu and by Nomland from Leyte were de-
scribed; in the later work, much additional ma-
terial, mostly orbitoidal. was described from
samples collected by W. D. Smith. R. E. Dick-
erson. W. E. Pratt. F. A. Dalburg. Graham
Moody. H. M. Ickis. H. D. McCaskey. A.
Kryshtofovich. F. Kearney, H. G. Schenck,
Father Sanchez, M. Goodman, and R. D. Row-
ley, from localities on the islands of Cebu. Ba-
tan. Rapu Rapu. Luzon. Masbate. Mindanao.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

Mindoro, Marinduque, Palawan, and Samar. In
Rowley's sample from Palawan, Yabe and Han-
zawa found the first Eocene large foraminifers
to be recorded from the Philippines: Discocylina
and Camerina .

From 1939 to 1941 the Philippine Petroleum
Survey added much data on Cenozoic foramin-
ifers, both large and small. These data were re-
corded and discussed in the light of the previous
literature by Corby et al. (1951: 227-297). The
Philippine large foraminifers previously record-
ed in the literature were listed, their ranges in
both Philippines and Dutch East Indies were
tabulated and their ages and correlations shown
on plate 31 of that report. A check list of pub-
lished Cenozoic and Recent small foraminifers
from the Philippines, prepared by Benjamin Dal-
eon with assistance from Mariano Herrera, was
presented as plate 32. The references to the sys-
tematics involved were tabulated in a bibliog-
raphy prepared by Juan S. Teves of the Philip-
pine Bureau of Mines, and this tabulation was
included in the final report of the Survey, but
due to the magnitude of the material covered,
his contribution was omitted from the part of the
report eventually published in the Corby et al.
(1951) report. A copy of this tabulation is now
on deposit at the California Academy of Sci-
ences.

Certain foraminiferal collections of the Survey
were also tabulated in the Corby et al. (1951)
report. To the extent that preliminary identifi-
cation of local type-specimens was possible
within the time limitations imposed by the im-
mediate aims and facilities of the Survey (ibid.:
229-231), their distribution in biostratigraphic
sequences selected as types for a local biochro-
nologic classification was shown on plates 34.
35, 39, 40, 41, 42 and 43. With the types sub-
sequently destroyed, most of the value of plates
35, 39, 40, 41, and 43 have been lost, though the
distribution of some genera — camerinids and or-
bitoids and "RotaliaS^ for example — has re-
tained certain significance, although the local
biochronologic terminology was never intended
for publication.- In the wake of the Philippine
Petroleum Survey, considerable additional in-
formation has been published. A chart of the
relative stratigraphic ranges of certain Neogene
smaller foraminifers in the Philippines has been
presented by Daleon ( 1958; see also Cook 1963,

See Note 2 in Appendix A.

fig. 4). Hashimoto (1939: table 1) had previously
proposed a stratigraphic classification for the
Philippines, listing both large and small foramin-
ifers from the series and formation of his clas-
sification, the former from 24 localities, the most
interesting of which are in the Cordillera Central
of northern Luzon, which had not previously
been realized to be productive of forms such as
Spiroclypeits margaritatus, S. vermicularis, and
Biphinispira mirahilis. Minute forms of foramin-
ifers are also listed from eight other localities
(ibid.: tables 3. 5; see also Kleinpell 1958: 9.
footnote 5).

Grey (1954, 1956) described and discussed the
occurrences of Eocene large foraminifers in the
Philippines, including previously unrecorded lo-
calities in Cebu, Mindoro, the Caramoan Pen-
insula, and in Albay, Luzon. Additional occur-
rences of Tertiary small foraminifers have been
recorded by Daleon (1951). Daleon and Saman-
iego ( 1954). Cook ( 1963). and Amato (1964).

Planktonic small foraminifers, together with a
few benthonic species, have been recorded by
Bandy ( 1963) and made the basis for a Neogene
zonation (ibid.: 1735, fig. 2, 3) based on sections
in southern lloilo, Panay, and in the central val-
ley of Luzon, where the two thickest and struc-
turally most unbroken sections and also the two
most continuously foraminifera-bearing se-
quences in the Philippines have long been
known. Oldest beds in Bandy's foraminiferal se-
quences are those from a subsurface occurrence
(Tigbauan well No. I) in the southern lloilo ba-
sin of Panay which he correlates with Globiger-
ina concinna ciparoensis Zone of the Caribbean
and with the Chattian Oligocene of Europe. The
bulk of Bandy's planktonic foraminifer faunas
are of Miocene, Pliocene, and Pleistocene age
(ibid.: figures 5, 7).

Philippine Stratigraphy and Correlations . —
Geologic and stratigraphic studies in the Phil-
ippines in recent years have added to the records
of Cenozoic fossils, mainly foraminifers. Irving
(1952, 1953) followed the letter symbols em-
ployed by Corby et al. (1951) who, in 1954,
pointed to the probable Indonesian correlates
(i.e., the "letter classification" equivalents) of
the local Philippine letter symbols. Vergara et
al. ( 1959) presented an areal geology map of the
Cagayan Valley north of Tuguegarao, together
with three graphic columnar sections from the
Cagayan Valley region, in a paper in which the
"letter classification" of Indonesia (the former

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Dutch East Indies) is brought directly into the
stratigraphy of northeastern Luzon. In view of
the bearing of Martin's study of Cagayan Valley
fossils upon Dickerson's evaluation of the Vigo
Group of the Bondoc Peninsula, the Neogene
column in the Cagayan Valley is worth further
discussion.

In 1954. the junior author, while engaged in
petroleum exploration for private industry, un-
dertook a study of the stratigraphy, paleontol-
ogy and structure of northern Luzon and espe-
cially of the Cagayan Valley, the geology of
which had. at that time, been left in essentially
the broad reconnaissance state of coverage of
the Philippine Petroleum Survey. Corby et al.
(1951: pi. 139) summarized the formation se-
quence as consisting, in ascending order, of the
Ibulao Limestone (Tertiary Upper and Lower
X). Callao Limestone (Tertiary Lower X). Tug-
uegarao Sandstone (Tertiary Middle X). Ilagan
Sandstone (Tertiary Lower Z). and Magapit
Limestone (Tertiary Z). They suggested that an
upper member of the Ibulao in a southerly area
(■"south of Jones"") was in possible lenticular re-
lationship with the generally overlying Lubu-
agan (ibid.: 210). and they recognized a local
unconformity between Tuguegarao and under-
lying Lubuagan (ibid.: 211). In subsequent stud-
ies of Kleinpell (1954).-* some revisions of the
local stratigraphy were found necessary. For
example, the Lubuagan. though locally rich in
carbonaceous material and even leaf impres-
sions, seemed more appropriately designated as
a formation than as "coal measures"": it ap-
peared divisible into three clastic members with
the Ibulao as a fourth and basal member of len-
ticular limestone (ibid.: 5. and correlation chart
between pp. 15 and 16). Kleinpell found the Cal-
lao Limestone to grade lateralh into sands pre-
viously mapped as Tuguegarao. and both were
in turn lateral equivalents of the middle and up-
per Lubuagan Formation (ibid.: 8). The Tugue-
garao Sandstone of previous mapping also, in
part, graded laterally into a portion of the Ilagan
Formation: at best it constitutes a cartographic
unit areally much more restricted than the for-
mation of that name as previously mapped. The
mapping of the Tuguegarao as a formation was
more than seriously open to question^ (ibid.: 10-
1 1 ) and perhaps v\ as due to an attempt to depict

^ See Note 3 in Appendix A.
■* See Note 4 in Appendix A.

areally clastic sediments of presumably about
the same age as deduced from scattered fossil
content. Kleinpell encountered no unconformity
between the Tuguegarao and Ilagan Formation,
the implied hiatus being not depositional but due
instead to the lack, or at least the scarcity of.
fossils definitely of upper Miocene. Mio-Pli-
ocene. or lower Pliocene age in the interval be-
tween fossiliferous middle Miocene below and
the "Upper Pliocene"" of previous correlations
above (ibid.: 1 1-12). The Ilagan. coarsely clastic
throughout in areas where it overlapped onto
crystalline basement complex (as for example in
the San Mariano region southeast of the com-
munity of Ilagan). included a local and lenticular
fine-grained clastic lower member (as. for ex-
ample, around Penablanca. west of Calao,
where the Pinacanauan de Tuguegarao flows for
some distance essentially due south through low
terrain between the more resistant Callao Lime-
stone on the east and Ilagan Sandstone on the
west) (ibid.: 12-14). The fossils which had been
the basis for considering the Magapit Limestone
as of "Tertiary Z"" age were mostly shells of
essentially Recent type from a shellbank im-
mediately above the limestone (ibid.: 14. foot-
note 38). Thus Kleinpell (1954: 5) presented a
revised stratigraphic column for the Neogene of
the Cagayan Valley:

Lagoonal and Terrestrial Deposits

Pleistocene

Ilagan Formation Pliocene

Transitional Beds .... Miocene to Pliocene
Lubuagan Formation Miocene

Kleinpell considered the former Ibulao Lime-
stone a member, basal and lenticular, of the Lu-
buagan Formation, and included under the des-
ignation Transitional Beds, the Callao Limestone,
the upper member and parts of the middle mem-
ber of the Lubuagan Formation (together with
local coarse elastics left as local residue, as it
were, of the unmappable Tuguegarao Sand-
stone), and a lenticular "lower Ilagan mud-
stone"" member.

The Miocene age determinations stemmed
principally from orbitoids found at the localities
shown in the Corby et al. report (1951: pi. 10);
these were of fl and f2 age (lower and middle
Miocene) but also included a number that were
of older Tertiary e4-e5 age. with Eulepidina
(scnsii stricto). \\ hich might better be considered
upper Oligocene or at least Oligo-Miocene in age

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

(Kleinpell et al.. 1934: 8-11). Pliocene determi-
nations were based on small-foraminifer assem-
blages (ibid.: 14) rich in Ammonia ["Rotalia"]
papulosa and close relatives, in keeping with
their consistent supraorbitoidal stratigraphic oc-
currences in the "Rotalia Zone"" of the East In-
dies (ibid.: 22), Panay."' Cebu,** and Leyte."
Pleistocene determinations stem from fossil
mammalian data (ibid.: 15; see also Beyer 1956.
and Koenigswald 1954. 1956). The oft-referred-
to guide fossil. Vicarya callosa. was not en-
countered in the Cagayan Valley above foramin-
ifer-bearing strata of Miocene age.

By 1957. in view of the revised stratigraphy,
it was possible* to relate this Cagayan Valley
Neogene sequence, both as to age and geologic
history, to the Tertiary sequence of the East In-
dies by the "letter classification" much more
closely and in greater detail than before; it was
also possible to include the results of compara-
tive studies, made with private funds in Ban-
doeng and Balik Papan late in 1940. between the
Philippine and East Indies foraminifer se-
quences (see Kleinpell 1958: 1-3). In 1940. it had
been possible only to write:

Were comparison with type material possible at present
... it is conceivable that the stratigraphic terminology of
the Netherlands East Indies could be employed in the pres-
ent report, and the currently employed local terminology
eliminated; thus geologic comparisons between the two
areas would be much more satisfactory as to detail. (Corby
et al. 1951: 294; see also pp. 295-2%]

Subsequently. 18 years later, it was possible to
add that

Upon examination of these faunal sequences in Balik
Papan it was immediately apparent that the Philippine Neo-
gene assemblages were in faunal facies nearest to those
from New Guinea and to some extent those from Java in
marked contrast to those from eastern Borneo, although in
nearby northern Borneo strong similarities of this sort again
were very much more apparent. It was also soon clear, as
had been previously suggested by comparative studies in
Bandoeng, that tentative correlations between the Philip-
pines and the southern Indies based on the larger-foramin-
ifers could on the whole be readily corroborated. A few
minor discrepancies between the ranges as previously pub-
lished and certain stratigraphic occurrences observed in the
Philippines remained. This was much as already noted by
Mrs. Harriet Williams Morrison in Manila (Corby et al..
1941; 1951; pp. 266-277); yet the latest data on the strati-
graphic ranges of nummulite and orbitoid subgenera and
species in the Indies seemingly called for no major modi-
fication of the "letter classification"' .... Again, in Balik

^ See Note 5 in Appendix A.
^ See Note 6 in Appendix A.
' See Note 7 in Appendix A.
* See Note 8 in Appendix A.

Papan, . . . classification of Miocene and Pliocene mollus-
can correlations . . . was greatly aided through compari-
sons of the associated small-foraminifer faunas ....

For example, small-foraminifers definitely of Tertiary hi
and h2 age in the Netherlands Indies were essentially those
of the typical Tertiary "Y"" and "Lower Z" intervals in
the provisional Philippine time-scale. In both regions, the
faunal sequences in question occupy a stratigraphic interval
characterized by a marked evolutionary diversification, and
a quantitative efflorescence as well, within the genus Ro-
talia l=Ammonia]. In the Philippines such newly appearing
rotalid species are exemplified by "Rotalia 2" through
"Rotalia 4" in the typical "Y" and "Lower 2" sequences
of west-central Panay [footnote 3: Corby et al. (1951: pi.
35 and also pi. 34 and p. 288)]. The basal horizon of the
interval in question corresponds to the base of the so-called
"Rotalia Zone." which has been widely employed as a key
horizon in reconnaissance exploration throughout the East
Indies and the Indo-Pacific province as a whole. This ho-
rizon generally is taken as the base of the local Pliocene
(see Kleinpell. 1954. p. 22). In the more southeriy Indies
it coincides with the base of hi — even somewhat below the
base of Tertiary g (Corby et al. 1941; 1951. p. 262). Many
factors were involved in these discrepancies in Pliocene
correlation. One of these had been . . . perforce . . . partial
analysis of incomplete data. Another ... in Borneo and in
the southern Indies generally the typical Tertiary g interval
is distinguished from immediately older and younger se-
quences principally on the basis of negative faunal features
alone. Too. examination in Balik Papan of the character-
istic Tertiary f3-Tertiary g-Tertiary hi small-foraminifer se-
quence soon revealed that the microfauna of Tertiary g
was represented in the Philippines by those faunules found
characteristically in the uppermost 'Upper X" marl, i.e.,
the small-foraminifer faunules within the local [Upper X"
but above the highest local orbitoids yet still below the
local] Tertiary Y' beds (Corby et al. 1951. pi. 35). . . .
finally, it was also apparent that the Philippine Upper Z"
assemblages were all post-Tertiary in terms of the letter
classification." Though some local and related problems of
faunal facies still remain unresolved, probably this provi-
sional "Upper Z" interval in the Philippines represents not
the Upper Pliocene Tertiary h2 equivalent but instead the
lowermost Quaternary, i.e.. the Lower Pleistocene. This
would, in turn, correspond to the so-called "folded Pleis-
tocene." which is also the east Asiatic "Villefranchian" of
some authors (see Movius 1944). [Kleinpell 1958: 2-6[

The mammal bones, artifacts, and tektites
found in the Pleistocene of the Cagayan Valley
between Laya and Tabuk strongly suggest that
the Philippine horizon of their occurrence may
be roughly correlated with the horizon of Pithe-
canthropus crcctiis in the so-called upper Trinil
beds of Java, though no bones of Java Man have
been found associated with them in the Philip-
pines (see Beyer 1956; Koenigswald 1954. 1956;
Kleinpell 1958: 13; Durkee and Pederson 1961:
160).

Passing over additional discussion of Eocene.
Oligocene. and Tertiary f2 faunas and correla-

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

EUROPEAN
STANDARDS

NETHERLANDS INDIES

PHILIPPINE ISLANDS

EUROPEAN
STANDARDS

Ser i es

Leupold and van der Vlerk

( 1931 ), after van der Vlerk

and Umbqrove

Provisional Local Terminology
Employed for Purposes of
Petroleum Survey Report

Ser i es

Stage

Zone

Stage

Ho locene

P 1 e i s tocene

P 1 ei s tocene

Lower P le i s tocene

Upper

P 1 iocene

Lower

P 1 i ocene

Unner Non-orbi toidal
^^^""^ Orbitoidal

Miocene

Middle

Mi ocene

Lower

Typical Upper, Middle, and
Lower, undifferentiated

"Pre-Upper W" ; barren of
small forami n i f ers , but
often orb i to i d-bear i nq

0 1 i gocene

Sample L-OB 260 from the
Coal Harbor limestone (see
pi . ki, facing p. 250) ;
"Lower W" Sample Mr-JH No.
15 from Mindoro (see pp.
265-266 and 267-270)

0 1 i gocene

Sample Bo-JH
No. 7 from
Bohol

(See pp.
268-269)

(Typical and
other und i f -
ferent ia ted
occurrences )

Eocene

Sample Ct-Ha
No . 5 from
Ca tanduanes

Eocene

Pa leocene( ? )

Sample M-GC
No. 8 from
Mi ndanao

Pa 1 eocene( ? )

Text-Figure 2. Correlation of provisional Philippine time-rock and Dutch East Indies letter classification.

tions between the Philippines and the more
southerly Indies (Kleinpell 1958: 6). and adding
data pertinent to Tertiary c of the Indies and
"V" of the Philippines, the summary chart of
correlation between the "'letter classification""
and the tentative classification of the Philippine
Cenozoic (Kleinpell 1958: 8) is reproduced here
as Text-figure 2.

These revised correlations, especially at the
late Miocene. Pliocene, and Pleistocene hori-
zons, affect the graphic summaries of the com-
parative geologic histories of the two regions
(Corby et al. 1951: pis. 12. 50; Irving 1952: fig.
3). Perhaps of at least equal interest and signif-
icance in this connection, however, is the rela-
tionships of the Cagayan Valley Neogene his-
tory to the rest of the Philippine Neogene as
indicated by the 1954-1958 revision of Cagayan
Valley stratigraphy. Post-1945 drilling in the
Visayan region had already shed additional light
on the same matter in the central Philippines
(see Daleon 1951) and by 1957 it was possible to
write that:

In northwestern Cebu, and on the Bondoc Peninsula of
southern Luzon, deposition appears to have been more
nearly continuous throughout Miocene time than in most
other nearby areas in the central and eastern Visayas.

Thus, the Neogene history both of northwestern Cebu and
of the Bondoc Peninsula appears to be almost as closely
related to that of Central Panay and of the adjacent north-
ernmost Negros coast as to that of the balance of central
and southern Cebu. northwestern Leyte, and southeastern-
most Luzon.

In northern Luzon conspicuously the Neogene deposi-
tional record is again more like that of central Panay. Both
surface and subsurface stratigraphic studies, carried on
since 1954 by Paul H. Dudley. Benjamin Daleon and the
writer, assisted by Mario Nieto. Jose Kanapi and others,
have demonstrated that throughout much of the Cagayan
Valley of northeastern Luzon deposition was essentially
continuous through Miocene and Pliocene time instead of
having been widely interrupted there during Upper Mio-
cene and Lower Pliocene times, due. as previously sup-
posed, to the local effects of the mid-Miocene (f2. or 'Mid-
dle X') orogeny in that area.

Thus, major tectonic lines and tectonic province-bound-
aries probably are. in detail, more sinuous in the Philip-
pines than as originally shown in the petroleum survey re-
port, with stronger east-west components. This now
appears to be more as in the Banda Arc. though on a small-
er scale. It is also in keeping with the postulate that the
modem Sulu-Mindanao and Palawan-Mindoro-Luzon to-
pographic alignments both reflect very ancient and long
prevalent structural and topographic features of a similar
position and orientation. In summary, it may therefore be
stated that a large part of the Visayan Sea and the Sibuyan
Sea lies within that historical-geologic belt termed 'tectonic
province II.' instead of in 'tectonic province 111' as previ-
ously shown (Corby et al. 1941; 1951; pis. 12, 50). In keep-

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

ing with the additional data from northeastern Luzon the
same may be said of the Cagayan Valley. [Kleinpell 19S8:
9-101

Thus in "tectonic province IT" north of North
Borneo, as early as Paleogene times, no contin-
uous depositional record is to be found from
Tertiary b to Tertiary c, though both stages are
present in separate areas there. Kleinpell (1958:
10-13) also noted that the major Cenozoic geo-
syncline more or less coinciding with "tectonic
province II.'" also reflected a paleogeographic
seaway which, waxing and waning in breadth
but ever present throughout Cenozoic time, was
at the root of the celebrated Oriental-Australian
life-zone boundary between Molengraaf's Sun-
daland and Papualand and known to zoogeog-
raphy as Wallace's Line. Miocene orogenies
probably played a role in the establishment of
the peculiarly transitional life-area of unstable
geologic history termed Wallacea. between Wal-
lace's Line and Weber's Line and including the
larger part of the Philippines. Celebes, and most
of the more westerly Lesser Sundas (see Dick-
erson 1928: 281-303. figs. 4. 16-28. 50. 56. 57.
60-64. pi. 40; see also W. D. Smith 1924;
Umbgrove 1938. 1949; Wisser 1940; Mayr 1944;
de Beaufort 1948; Beyer 1948. 1955; von Koen-
ingswald 1956). From a purely physical stand-
point it had been previously

. . . possible to extend the northward recognition of the
axis of this ancient Tertiary marine trough from the north-
em end of Makassar Strait to south-central Panay. There
its traces seemed to emerge from the depths of the modern
Sulu Sea; and thence, to all appearances, it extended north
via Verde Island Passage, between Mindoro and Luzon,
and, by way of the Manila Plain and Lingayen Gulf, on
north into the South China Sea. Post-war studies in north-
em Luzon, however, have suggested that north of the Vi-
gan region, the marine Neogene Lingayen basin passes in-
land rather than seaward, that many of its sedimentary
deposits grade laterally there into pyroclastics and volcan-
ics, and that its axis then rises northward above the older
crystalline rocks of northern Abra Province. Rather, it is
now indicated that the modem Cagayan Valley reflects the
northward continuation of the belt of most continuous Neo-
gene deposition.

Paleogeographically, the old Cagayan depositional basin
apparently connected with the former Tertiary trough of
the Manila Plain by way of the western Ifugao foothills
and the region of Balete Pass. This connecting area is one
which subsequently has been strongly folded, uplifted, and
then covered with Quaternary pyroclastics. Outcrops of the
older marine limestones and elastics of the Tertiary, all
strongly deformed, are limited to sporadic 'windows" in the
younger volcanics, as in the vicinity of Kiangan. of Balete
Pass, and of the Carranglan Valley in Nueva Ecija. [Klein-
pell 1958: 12-13; and see Corby et al. 1951: pis. 9. 10]

Durkee and Pederson (1961) greatly extended
the previous stratigraphic studies of the Cagayan
Valley and of the area west of the Cordillera
Central of northern Luzon. Following a prece-
dent established by Abadilla (1931) in northern
Panay and employed in the Baguio district of
Luzon by Leith (1938) and later by the Philip-
pine Petroleum Survey (the procedure originally
had been employed by W. D. Smith (1906). Fer-
guson (1909. 1911) in Masbate. and Pratt and
Smith (1913). but had subsequently fallen into
disuse). Durkee and Pederson gave a number of
local mappable stratigraphic units in the Cagayan
Valley new names as well as selecting and des-
ignating type sections. Except for the Callao
Limestone, such typology had been omitted in
previous reconnaissance mapping of the area.
They measured and described these type sec-
tions in great detail.''

Future work may make it advisable to con-
solidate some of these local formations but. for
the present, they serve admirably to clarify the
distinction between fact and interpretation. For
example, in discussing the southward disap-
pearance of the Sicalao Limestone along the east
side in the vicinity of Salegseg. Durkee and Ped-
erson (1961) considered this as possibly due to
Post-Sicalao and pre-Macaba River Group fault-
ing and stripping, whereas lenticularity is as
ready a possibility, since fossiliferous limestone
stringers of this same age are interbedded with
elastics of the Lubuagan Formation at several
localities in the middle Chico River-Lubuagan
region.'" Stratigraphically higher elastics with
even younger orbitoids" were found in subsur-
face sequences (the Tumauini wells) farther
south to have lensed southward into very fine-
grained siltstones and silty mudstones carrying
not the inshore orbitoids but their offshore-fa-
cies. small-foraminifer age equivalents. Much of
what the authors accurately referred to as serv-
ing to "further muddle the concepts of the stra-
tigraphy along the western margin of the Cagay-
an Valley" (Durkee and Pederson 1961: 150)
stems from failure to distinguish differences
within biofacies in the course of correlation.
Meanwhile, even lithofacies change has been
picked up only very slowly in this same area,
though Durkee and Pederson were meticulous
in this matter. One may question the worth of

" See Note 9 in Appendix A.
'" See Note 10 in Appendix A.
" See Note 1 1 in Appendix A.

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

replacing with the term Macaba River Group,
the old term ■'Lubuagan Formation"" — certainly
it was anything but a "'coal measure,"" and cer-
tainly it had no specified type section, nor would
it be likely to have a very good one, except as
a ■ "group"" or as a formation with its members
more clearly defined elsewhere. Whether or not,
in an area of overturning and isoclinal folds such
as that around Naneng. it actually does attain a
thickness of 8200 m (ibid.: 151), in our view, it
is these authors" handling of the highly lenticular
stratigraphy of the Cagayan Valley with a dis-
creet and carefully disciplined terminology that
will serve in the end to clarify the biofacies as
well as the lithofacies problems involved there.

Occurrences of large foraminifers. such as
Camerina (presumably in "derived" form, from
the basement complex on Capilyan Creek about
five kilometers south of the Tumauina River
along the east side of the Cagayan Valley). Eii-
lepidina and a few others, at least by implica-
tion, are noted by Durkee and Pederson. The
formations described and discussed are corre-
lated directly with the East Indies "letter clas-
sification"" as well as with the local letter ter-
minology of the Corby et al. report, as they are
also in a correlation chart of nine Cagayan Val-
ley columnar sections with, in addition, one
from the west side of the Cordillera Central in
which most of the extant terminology (Kennon
Limestone. Tertiary e4-e5 to fl; Twin Peaks
Formation. Tertiary fl-f2; overlying Klondyke
Conglomerate, tentatively Tertiary f2. on the
basis of superpositional relationships with fos-
siliferous underlying and overlying formations:
and Rosario Formation. Tertiary 13 to probably
h2) is retained.

Beyond the wealth of detail, one other obser-
vation by Durkee and Pederson is of great sig-
nificance for the stratigraphy, paleontology, and
Cenozoic history of the Cagayan Valley in par-
ticular and the Philippines in general: the like-
lihood that the crystalline basement complex in
and around the Cagayan Valley is of Tertiary
rather than of pre-Tertiary age (ibid.: 148. 154).
Their postulate is in keeping with the demon-
stration by Wisser ( 1940) that the Tertiary Vigo
Group in the nearby Baguio district of northern
Luzon, has been intruded by quartz-diorite. The
youngest strata invaded by diorites at various
points are of Tertiary fl age (see Corby et al.
1951: 102-103); similar implications of extensive
Tertiary f2 diorite intrusion are indicated by or-

bitoid-bearing intruded metamorphics in the
Paracale mining district of Camarines.

It will be recalled that criteria for the original
recognition by Dickerson of the Miocene age of
the Vigo Group molluscan fauna from the Bon-
doc Peninsula consisted of the relevant geologic
history, stratigraphy, larger foraminifers. and
relationships of the mollusks themselves to fos-
sil mollusks elsewhere, especially those of Java.
With the Neogene of Panay. northern Cebu.
northwestern Leyte. the Singayen region, and
Cagayan Valley subsequently brought into much
closer relationship to each other, to that of the
Bondoc Peninsula, and to that of the East Indies
generally, and with even details of both biofacies
and lithofacies coming to be clarified over a wide
terrain, it is appropriate at this point to view the
Vigo Group molluscan fauna within the context
of this subsequently gathered data.

AGE AND CORRELATION OF THE VIGO
GROUP. BONDOC PENINSULA. LUZON

A. On the Basis of Foraminifera and Bio-

STRATIGRAPHIC SUPERPOSITION

Stratigraphy . — Summary descriptions or de-
pictions of the Neogene stratigraphic sequence
in the southern Bondoc Peninsula have appeared
at least four times in the literature. The earliest
description was that of Pratt and Smith (1913)
whose detailed descriptions of the Vigo Shale
and the Canguinsa Sandstone were modified by
those of W. D. Smith (1924: 80-83). Pratt and
Smith"s (1913) description of the sequence may
be summed up about as follows:

Malumbang Formation. More or less coralline
limestones, calcareous sandstones and marls,
concordant and locally conformable on the
highest underlying formation in synclinal
areas, and widely transgressive.

a. Upper Limestone Member 30 m

b. Cudiapi Sandstone Member 40-135 m

c. Lower Limestone Member. 20 m

Canguinsa Sandstone. Close-grained, gray or
blue sandstone, more massive than the Cudi-
api Member of the Malumbang and character-
istically with a considerable proportion of
clay. Upper portion usually a soft, clayey
sandstone, calcareous, occasionally close
jointed and concretionary. Lower portion
either a deep blue typical sandstone that

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

weathers gray or brown, or an indurated mas-
sive or jointed blue clay that weathers gray.

"In the section on lower Bahay River, the
Canguinsa sandstone includes a few meters of
limestone and conglomerate. On Mount Mag-
lihi and Mount Morabi limestone which con-
tains coarse sand and small pebbles of diorite.
quartz, and andesite is present in the Can-
guinsa sandstone, but no conglomerate was
observed. [Ibid.: 329]

"No definite age determinations can be
made from the fossils in the Canguinsa sand-
stone proper. The fossils in the included lime-
stone, however, are well known and have
been used in correlation by various authori-
ties. From their presence it is concluded that
the Canguinsa sandstone should be placed in
the middle Miocene, extending, perhaps, into
the lower Miocene." [Ibid.: 330]

50-160 m

Vigo Shale. Fine-grained gray. blue, or black
shale and sandy clay shale interstratified in
thin regular beds from 5-10 cm thick, with oc-
casional beds of gray or brown sandstone
varying from 10 cm to 1 m in thickness; pet-
roliferous, especially in upper 50-75 m which
have fewer sandstone beds, are more massive
and conchoidally fracturing — the so-called
"Bacau stage."

"There is an apparent transition from east
to west in the character of the Vigo shale. In
the eastern limb of the Central anticline, ex-
posed in the valley of Vigo River, the forma-
tion is predominantly shale throughout, sand-
stone occurring only at intervals. In the
western limb shale predominates in the ex-
posure near the axis only, that is. the lower
part of the series. Farther to the west the
sandstone beds increase in number, until in
the upper horizons they become more prom-
inent than the shale. The grain-size likewise
increases in the upper beds, and small pebbles
occur, forming layers of sandy conglomerate.
[Ibid.: 3311

"... In the eastern half of the field, the
Canguinsa sandstone overlies the Bacau stage
in a majority of exposures. Occasionally . . .
sandstone and fine conglomerate, which are
evidently a part of the Vigo series, occur
above the Bacau stage. In the western part of
the peninsula sandy conglomerate is found
near the top of the Vigo formation. These

overlying beds may be always present above
the Bacau stage, but concealed generally by
an overlap of the unconformable Canguinsa
sandstone.

". . . The thickness of the Vigo is unknown.
An apparent thickness of about 1 .400 meters
is revealed in the Matataha River section, the
section on Malipa Creek in the southern limb
of the Malipa anticline shows 800 meters of
Vigo shale, and the section on Guinhalinan
River indicates 600 meters. None of these sec-
tions exposes the base of the formation. The
apparent thickness of the sections as mea-
sured along the outcrop may be in excess of
the actual thickness as a result of superficial
expansion of the beds or of the repetition of
beds from faulting or close folding." [Ibid.:
332-333]

1400+ m

Dickerson (1921a: 2-3) described the Mal-
umbang as up to 1000 feet (305 m) thick and.
referring his readers to the "strata referred by
Pratt and Smith to the Canguinsa formation and
Vigo group. ..." sums up:

The oldest rocks here recognized consist of shales and
sandstones from 3000 to 4000 feet in thickness, the Vigo
group and its uppermost member, the Canguinsa formation.
The strata as exposed in the vicinity of the Vigo River are
steeply dipping, black, organic shales, subordinate sand-
stones, and minor lignitic strata which are unconformably
overlain by the Malumbang formation. . . .

Dickerson added in a footnote that his "view
concerning the stratigraphy of the region under
discussion differs in this regard from that of
Pratt and Smith, but a full exposition of this im-
portant point cannot be given here." Subse-
quently, he (Dickerson /'// Smith 1924: 313) ex-
plains:

I am not in agreement with Pratt and Smith concerning
the stratigraphic relations of the Malumbang. Canguinsa.
and Vigo in their type localities. Bondoc Peninsula. I be-
lieve that a great unconformity exists between the Mal-
umbang and the underlying Vigo group. I failed to recog-
nize an unconformity between the Canguinsa formation and
the Vigo shale, although the areas cited by Pratt and Smith
were critically examined. The relations that appear at these
places are best explained by faulting. On this account, the
term "Vigo" is widened to include the Canguinsa forma-
tion as its upper sandstone facies. thus raising the term
Vigo to a group rank.

With the exceptions noted. Dickerson essential-
ly follows the stratigraphy of Pratt and Smith.
In the Corby et al. report of 1951. a graphic

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

cross section (ibid.: pi. K) along Bacal Creek
across a faulted anticline shows the following
sequence:

Malumbang Formation Unconformity

Upper Canguinsa
Bacau "stage"
Lower Canguinsa

About 600 ft

(200 m)
About 750 ft

(225 m)
About 250 ft
(76 m)
Maglihi Lime and Sandstone About 1250 ft

(380 m)
Molave Gravels About 250 ft

(75 m)
Vigo Shales ("Upper Vigo") Undetermined

thickness

The thickness of the Maglihi Lime and asso-
ciated sandstone, and of the Molave Gravels are
considerably greater than those of comparable
units of the Vigo in Pratt and Smiths' work and
are probably more accurate. More detailed map-
ping in the area permitted recognition of more
members, both of the Canguinsa and of the Vigo
formations. Allowing for a maximum of 1400 m
of exposed Vigo (Pratt and Smith 1913). or from
914-1219 m (3000-4000 ft) of exposed Vigo
Group (the combined Canguinsa and Vigo of
Dickerson 1921, 1924), a thickness of about 760
m (2500 ft) of Vigo Shales below the Molave
Gravels appears to be a maximum thickness of
these shales in outcrop. In view of the twice-
modified rock-stratigraphic terminology in use
by 195 1 . it should be noted that the Bacau Mem-
ber ("stage" of Pratt and Smith, "local facies.
and its position not uppermost" of Dickerson
fide Smith 1924:81) is the "middle Canguinsa"
of the Corby et al. (1951) report, with some 76
m (250 ft) of sandstones mapped as Canguinsa,
though not included within that formation by
Pratt and Smith. It seems also significant to add
volcanic agglomerate, a single small outcrop of
which occurs at the base of the Bacau and again
at Pratt and Smiths' "unconformity" at the base
of their Canguinsa. To repeat, the base of the
Vigo Shales is not exposed on the southern Bon-
doc Peninsula; the stratigraphically lowest beds
are those exposed in the core of a closed, but
generally southward plunging, anticlinorium
(see Corby et al. 1951: pi. 26; Irving 1953: map
section 11). To the north, on the Tayabas
isthmus, the lowest or "Tayabas coal mea-
sures" formation (with limestones, brown car-

bonaceous sandstones, and gritty calcareous
sandstones) is a more-or-less comparable strati-
graphic sequence (Tayabas-Aloneros Con-
glomerate— Hondagus Silt — Sumulong Diatom-
ite — Vinas Formation — Malumbang Formation).
It is intensely folded and appears to lie with
depositional contact upon schist and gneiss along
the north coast of the isthmus opposite Alabat
Island (Corby et al. 1951: 192-195).

Cloud ( 1956: pi. 1) presented the following se-
quence for the Neogene of southeastern Luzon:

Malumbang Is. (after Dickerson) . 10(V-200 ft
Canguinsa fm.

marl. Is., sh.. sdy marl 500-1200 ft

Maglihi s.

calc. s 1000-2000 ft

Molave eg. 100-400 ft

Vigo fm.

mainly sh. and ss. 1450 ft plus

Biostratigniphy of the Foniminifers . — "The
oldest fauna yet recorded from the Vigo area is
the orbitoid assemblage from a piece of float on
Bahay River reported by Yabe and Hanzawa as
Pratt's locality No. 3" (Corby et al. 1951: 282.
pi. 31. locality no. 177). The orbitoid is Lepi-
docyclina (Eulepldina) formosa Schlumberger,
a species not known from strata younger than
Tertiary e5. This eulepidine. sensH stricto. is
probably conspecific with Lepidocyclina richth-
ofeni Smith, and is perhaps the form in the lime-
stone from Mount Morabi referred to the latter
species by W. D. Smith and cited by Dickerson
(1921a: 14-15). although the species was not
found in place in any of the strata on Mount
Morabi by the Philippine Petroleum Survey (see
Corby et al. 1951: 286). The eulepidine would
permit a correlation with at least a part of the
Cebu Limestone which carries L. {E.) formosa,
as discussed by Yabe (1919) and cited by Dick-
erson (1921a: 15). Its actual stratigraphic occur-
rence in the Vigo area is not known, however,
and concerning this sample of fossiliferous float,
it is only possible to repeat, "This material was
probably derived from the Vigo formation,
though not assuredly so. and it is apparently of
Upper W age" (Corby et al. 1951: 282). i.e..
Tertiary e4-e5. and thus Oligocene (see Dick-
erson 1921a: 16), or at least Oligo-Miocene stra-
ta are present at some unknown horizon within
the Vigo Group of this area.

Small foraminifers in the Vigo Shale from be-
low the Molave ("Morabi") Gravels point to a

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

similar conclusion; none appear to indicate an
age younger than Tertiary f l-f2. and they permit
correlation with the Malumbang Formation-Mt.
Uling Limestone-Toledo Formation sequence
of Cebu stratigraphically above the Cebu Lime-
stone, the Singit Formation-Lower Tarao For-
mation sequence of Panay (see Corby et al.
1951: pis. 34. 35; and Bandy 1963). and with the
Tagnacot Shales of Leyte. which are strati-
graphically below the limestone with Lcpidocy-
clina V'Tiybliolcpidinif) rutteni of Tertiary f3
age.

Moreover, the orbitoidal limestone included locally with-
in the Canguinsa by Pratt and Smith . . . and hy Dickerson
. . . does not outcrop at the type locality of the Canguinsa
formation, and in fact stratigraphically underlies any beds
there exposed. Pratt and Smith note its absence in the more
northerly section of Vigo and Canguinsa on Bondoc. In the
present report, it is given the name Maglihi limestone he-
cause of its well-defined occurrence on Mount Maglihi.
LepidocycUna richthofeni .' reported by Smith . . . from
this limestone, and upon which rests the Miocene age de-
termination of Dickerson's Vigo moUusks . . . has not been
found, nor have additional specimens of this species been
found, in this in the field. However, numerous specimens
of large Foraminifera of similar generous dimensions have
been found locally. Microscopic examination has revealed
that the bulk are specimens ofCycloclypeus: others appear
to represent a large species of LepidocycUna (Trybliolepi-
dina) an orbitoid which, like Cycloclypeus. is known else-
where from Upper X limestone. Finally, it should be em-
phasized that his orbitoid horizon not only does not
represent the Upper W horizon of the Cebu orbitoid lime-
stone of Cebu, but also that it conformably underlies the
base of the Canguinsa, a formation here over 600 meters
thick, in the very uppermost beds of which occur the "Vi-
go"" mollusks reported by Dickerson. . . . [Corby et al.
1951: 286-2871

The orbitoids from the Maglihi Limestone are
stratigraphically the highest found to date from
the typical Vigo-Canguinsa sequence, and they
indicate a Tertiary f3 (orbitoidal "Upper X"")
age. Small-foraminifer faunas from the overlying
lower Canguinsa (of Corby et al.. not of Pratt
and Smith) and Bacau are meager, and some of
them indicative of brackish-water deposition;
evidence as to their age is more negative than
otherwise, suggesting though not indicating a
situation characteristic of Tertiary g (postorbi-
toidal "Upper X") throughout the archipelago.
Thus, the Vigo-Canguinsa sequence as high as
the orbitoidal horizons of the Maglihi Limestone
Member (Tertiary t3) is clearly of Miocene age.
Above this point evidence as to age is negative.

On the Bondoc Peninsula, the Upper X faunas of the
lower Canguinsa and Bacau . . . are succeeded upwards by

the Y faunas of the upper members of the Canguinsa.
Above the Y faunas is a thin limestone bed used as a key
horizon in mapping structure in the area, and above this,
still in the upper Canguinsa, are the fine-grained and richly
fossiliferous beds from which Dickerson"s "Vigo" mollusks
were collected. Both the mollusks and the small foraminif-
era from this uppermost Canguinsa are typical of the Lower
Z of Panay. [Corby et al. 1951: 2901

Translating the local letter symbols into the
stages and zones of the East Indian "letter clas-
sification." "Upper X" reads Tertiary f3 and g,
"Y" Tertiary hi. and "Lower Z" Tertiary hi.

A recent systematic study (Cook 1963) of the
small-foraminifer assemblages at these upper
Canguinsa localities has served to corroborate
and emphasize the Tertiary h age of the strata
at these localities. Seven samples from upper
Canguinsa localities are rich in the species of
"Rotalia" characteristic of the "Rotalia Zone"
Tertiary h. including Dickerson's locality 2x
which, with his 3,\. occupy the stratigraphic po-
sition of those molluscan faunas upon which his
percentages of extinction are derived. They are
horizons high in the Canguinsa and most prob-
ably well above the top of the highest Bacau
beds,'-

Thus. independent evidence from the fora-
minifers. both direct and indirect, indicates a
Pliocene age for the strata of the Canguinsa For-
mation of Pratt and Smith (the upper Canguinsa
of Corby et al,) including the horizons yielding
the mollusks of Dickerson's Vigo-Group fauna.
It remains to review, in the full light of Martin's
comprehensive studies of the mollusks of Java,
the direct evidence from the Vigo-Group mol-
lusks themselves.

B. On the Basis of the Mollusks

The Fauna. — Dickerson's theory concerning
the relatively slow rate of evolution of marine
tropical faunas was derived from study of col-
lections that he made from Tertiary beds ex-
posed in the Bondoc Peninsula. Luzon. These
collections were later brought to America and
deposited in the paleontological museums of the
California Academy of Sciences. San Francisco,
and the University of California at Berkeley and
have been made available to us. In addition to
Dickerson's original material, we have studied
collections from three Bondoc Peninsula locali-
ties made in 1937 by W. P. Popenoe while work-

See Note 12 in Appendix A.

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

ing for the Far East Oil Development Company
of Manila. Two of the three localities. CIT 1388
and 1389. are the same as Dickerson's localities
2x and 5x. respectively. Dickerson's localities
3x. 4x and 1 Ix v\ere not duplicated in Popenoe's
collections, and CIT 1390 is new. Dickerson's
locality 9x. being far removed from the others
and of dubious relationship to them, was not
used.

One hundred forty-nine species of gastropods
and bivalves are listed in the accompanying
checklist with approximate abundance of indi-
viduals of each species, reported geologic oc-
currence from areas outside of the Bondoc Pen-
insula, and notes and references from the
literature and from museum collections giving
authority for the identifications. With tv\o or
three exceptions, all of the species listed are also
figured with full locality and dimension data.
Most figures of specimens are magnified two or
three times.

Identification of the molluscan species has
been made with aid of the references listed, and
by direct comparison of the Bondoc Peninsula
fossils with Recent specimens in the collections
of the Department of Mollusks. U.S. National
Museum, and of the Department of Geology.
University of California. Los Angeles. Nomen-
clatorially. genera have been used in a broad
sense, subgenera and subspecies have not been
recognized, strictly nomenclatorial problems
have been avoided, and the synonymy presented
makes no claim to completeness, but lists only
those references recently published and readily
available that were used for identifications.
Broadly, the classification of Wenz has been em-
ployed for the gastropods, and the Bivalvia are
classified according to the plan in Part N. Trea-
tise on Invertebrate Paleontology .

Any criticism of the Dickerson theory on the
evolutionary rate of molluscan faunas in the
tropics must consider two questions: first. Are
the mollusk-bearing beds of the Bondoc Penin-
sula Miocene in age?: second. Are the contained
fossil faunas made up of species of which ap-
proximately 759?^ are still living? We believe that
Dickerson was incorrect in concluding that the
beds are of Miocene age — they are much young-
er. Most of the reasons for this opinion have
been expressed earlier in this paper, though
some discussion dealing specifically with the
supposedly extinct species will follow. Dicker-
son's conclusion that the faunas are made up of

approximately 759f Recent species, we believe
is approximately correct. This will be pointed
out in the analysis of the information assembled
in the faunal checklist.

In his first paper concerning the Bondoc Pen-
insula faunas. Dickerson (1921a: 12) wrote: "Tn
the above list there are 98 forms that are spe-
cifically determined, and of these 74 or 75.5%
are living species, an astonishing number when
the geologic history of the region yielding these
forms is considered. In addition, the extinct
forms are practically all common to the upper
Miocene of Java, according to K. Martin [1880:
44-51]." Dickerson (1921a: 10-12) listed the fol-
lowing supposedly extinct species:

Actaeon reticulatus Martin
Buccinium simplex Martin #*
Cerithium jenkinsi Martin
Cerithium herklotsi Martin
Cerithium bandongensis Martin
Cerithium jonkeri Martin #*
Cerithidea ne'dv dohrni? #*
Conus ornatissimus Martin
Conus hardi Martin
Conus striatellus Jenkins #
Columbella bandongensis Martin
Mitra Javana Martin
Mitra ct\ jenkinsi Martin #
Mitra junghuhni Martin
Mitra bucciniformis Martin
S trombus (Dfususl Martin
Turris coronifer Martin #
Terebra bicincta Martin
Terebra Javana Martin
Trivia smithi Martin # '
Voluta cf. inne.xa Reeve #
Corbula socialis Martin
Psammobia cf. lessoni Blainville #*
Vermetus javanus'l Martin #'

It was not explicitly stated that the presence
of these species in the Bondoc fauna was evi-
dence of Miocene age. but the inference is dif-
ficult to avoid.

Specimens representing these species, with
the exception of those starred, were later figured
by Dickerson ( 1922: pis. 2-7) and the hypotypes
w ere deposited in the collections of the Califor-
nia Academy of Sciences. Through the courtesy
of the late Dr. Leo G. Hertlein. Curator Emer-
itus of Invertebrate Paleontology at the Acade-
my, we have been able to borrov\ these hypo-
types for study and refiguring (see pis. 17 and

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

Table 1. Fourteen Species from the Vigo Group. Dickerson's (1921a) identifications in the first column, our identi-
fications in second column. Figure numbers refer to illustrations of conspecific specimens on plates 1-16. Geological age ranges
compiled from the "Feestbundel" and from works of Oostingh, Regteren Altena, MacNeil, and Shuto.

Dickerson's Identifications

Identification Used in This Paper

Figure

Known
Age Range

1. Aclaeon reticulatus Martin

2. Cerithium jenkinsi Martin

3. Cerithium ht-rklotsi Martin

4. Cerithium bandongensis Martin

5. Conus ornatissimus Martin

6. Conus hardi Martin

7. Cohonbella bandongensis Martin

8. Mitra javana Martin

9. Mitra junghuhni Martin

10. Mitra bucciniformis Martin

!1. S trombus {"?) fusus ? Martin

12. Terebra bicincta Martin

13. Terebra javana Martin

14. Corbula socialis Martin

Pupa sulcata (Gmelin)

Cerithidea jenkinsi (Martin)

Cerithium jonkeri Martin

Not found

Conus socialis Martin

Conus loroisii Kiener

Parametaria philippinarum (Reeve)

Vexillum vulpecula (Linnaeus)

Mitra interhrata Reeve

Vexillum cruentatum (Gmelin)

Not found

150

Recent

U. Mio-Rec.

26.27

Plio.

134. 138

U. Mio-Rec.

142

L. Mio-Rec.

71, 72

U. Mio-Rec.

114

Plio-Rec.

105

U. Mio-Rec.

109

U. Mio?-Rec,

18), with the exception of those indicated by the
#-symbol, which could not be found. Compar-
ison of Martin's illustrations of the species (re-
produced on some plates) with illustrations of
the inferred identical species from the Philip-
pines raises doubts as to the correctness of
Dickerson's identifications and the validity of
his stratigraphic correlations.

Listed in Table 1 are the fourteen hypotypes
figured on Plates 17 and 18. In the first column
are Dickerson's identifications of the forms; in
the second, our identifications are listed, fol-
lowed by the figure number of conspecific spec-
imens illustrated on Plates 1 to 16; and in the
final column the inferred geologic ranges of
these species are compiled from the "Feestbun-
del" and from the subsequent works of Oos-
tingh, Regteren Altena. MacNeil and Shuto.

Nine species for which geologic ranges are in-
ferred are included in Table 1. All except one
have been recognized from the Recent faunas.
Six are reported from beds of Miocene age.
though none is restricted to that epoch. Only
one — Cerithium jonkeri — appears to be extinct.
Thus, the assemblage as a whole implies only a
Neogene and not Miocene age. and correlation
with the fauna from Junghuhn's locality "O."

In summary, it is held that none of the evi-
dence put forward by Dickerson to demonstrate
the Miocene age of the Bondoc Peninsula mol-
luscan faunas has been sustained by later work,
and the inferred correlations and substructure
for the theory that molluscan evolution in the

tropical Pacific is slower than in temperate re-
gions are without foundation.

The question may next be asked: Does any
evidence exist as to the age of the Bondoc Pen-
insula faunas relative to those found elsewhere
in the western Pacific, and to the standard Cen-
ozoic time scale based upon type faunas from
western Europe? At least a partial and tentative
answer to this question will be attempted below.

Two systems for correlation are in common
use in western Pacific Tertiary biostratigraphy.
The first, based commonly upon analysis of the
molluscan faunas, expresses the ages of fossil-
iferous beds in terms of the standard epoch ter-
minology of western Europe — Eocene. Oligo-
cene, Miocene, etc. The actual stratigraphic
succession of the most prolific faunas is hard to
determine in most cases, and the faunal succes-
sion has therefore been inferred upon determi-
nation of the percentage of Recent species pres-
ent in the faunas according to methods
originated by Lyell and modified for use in In-
donesia by Karl Martin. This method of age de-
termination has been used generally by other
molluscan paleontologists working with Indo-
nesian mollusk faunas, e.g.. Tesch. Oostingh,
Regteren Altena. MacNeil and Shuto. All have
recognized that the Cenozoic epochs used in In-
donesia are not necessarily exactly equivalent
with those of the type sections in western Eu-
rope.

The second system of biostratigraphic classi-
fication is the letter system of Leupold and van

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

der Vlerk (1927) and is based principally upon
the succession of larger foraminifera. with more
recent utilization of smaller foraminifera as well.
The two types of classification have not been
completely satisfactorily integrated nor has
either as yet been satisfactorily coordinated with
European and American Cenozoic divisions. In
the discussion that follows, Cenozoic epoch
terms will be employed in the sense that they
have been used by Karl Martin and later pa-
leontologists working with western Pacific mol-
luscan faunas.

The faunal chart (Text-fig. 3) accompanying
this report lists 149 species of gastropods and
bivalves, comprising all forms believed to be
specifically determinable. We identified 127 spe-
cies; the remaining 22 were either considered as
conferred, or as undetermined, but not indeter-
minate species. There are 105 species, including
those questionably identified, that are believed
to be still living. A few unidentified species are
listed as still living because of their presence in
collections of Recent shells in the U.S. National
Museum.

Dickerson calculated the percentage of Re-
cent species as the proportion of identified forms
in the fauna; on this basis, the fauna in our check
list is 83% Recent, calculated to the nearest
whole percent. This figure is slightly more than
the 75% calculated by Dickerson. Neither figure
includes the fairly large proportion of undeter-
mined species, and there is no compelling reason
to think that the percentage of Recent forms in
the undetermined fraction of the fauna is nec-
essarily the same as in the determined fraction.
It might be argued that the percentage of extinct
forms in the 22 undetermined species in the
checklist would probably be greater than in the
determined species because the fossil molluscan
fauna of the Philippine area is poorly known,
whereas the Recent faunas of this region have
been much better described and figured, and be-
cause the collections of Philippine Recent mol-
lusks in the U.S. National Museum, consulted
in the course of this study, are among the best
in the world. For this reason, percentages of
Recent species in the following calculations are
based upon the total number of species in the
fauna, assuming in the first figure that all uni-
dentified species are extinct, and in the second
that they are all living. The two figures thus giv-
en indicate essentially the minimum and maxi-
mum percentages of Recent species in the fau-

nas. For the composite fauna, these figures are
70-85%.

For the discussion below of the Bondoc Pen-
insula faunas, the assemblages from the three
most prolific localities are analyzed and tabulat-
ed separately as to specific abundance, propor-
tion of Recent species, and the known time
ranges of the various species. The data for these
analyses are taken principally from the "Feest-
bundel," and are supplemented by information
from subsequent publications by Oostingh, Reg-
teren Altena, MacNeil, Shuto, Cossmann, Ab-
bott and Powell. Data for the three most prolific
localities, 2x-1388, 3x and Ilx are furthermore
expressed graphically on Text-fig. 4.

These data and graphs show that: (1) All lo-
calities have a considerable number of species
whose ranges begin in lower Miocene or in up-
per Miocene time. Such species make up from
27% (loc. 1390), to 55% (loc. 1389) of the total
species in each locality. Only two species of the
total fauna, however, are not found in beds later
than Miocene elsewhere in the western Pacific
Tertiary faunas. These two are Pot amides sn-
caradjctnus Martin, known elsewhere by a single
specimen from the upper Miocene of Java, and
Crassispira cf. C. hataii MacNeil. which is
found in a single locality in the Yonabaru Clay
Member of Okinawa. (2) All of the Bondoc Pen-
insula localities yield species whose ranges be-
gin in the Pliocene and are either elsewhere
known only from beds of that series or range
higher. The percentage of such varies from 54%
( I Ix) to 72% (3x & 1389). All of these localities
have a small number of species, from 1 to 6, that
are elsewhere found only in Pliocene beds. (3)
Several, but not all, of the Bondoc Peninsula
localities include species whose ranges begin in
beds of Pleistocene age. The greatest number of
such species is three, from locality 1 Ix. (4) All
of the Bondoc Peninsula collections contain
identified species that have not hitherto been
found as fossils. The percentage of such to the
total fauna ranges from 16% (9 species) in lo-
cality 3x to 3 1% (8 species) in locality 1390. Rec-
ognition of these species for the first time in the
fossil record obviously contributes nothing to
determination of the age of the containing beds.
(5) All localities yield a large proportion of spe-
cies known as fossil but still found living in Re-
cent seas. It has been pointed out earlier that it
is not possible to obtain precise figures for the
percentage of Recent species in each locality so

CLASS GASTROPODA

SUPERFAMILY TROCHACEA

SUPERFAMILY NERITACEA

SUPERFAMILY CERITHIACEA
. ArchHectonica perspecfiva (Linnoeus)

Architectontca maxima (Philippi)

Teiescopium tetescapium ? (Linn)
' Potamides sucaradjanus Martin

"Potamides" sp. 0

Cenfhidea ? sp-

Cenfhidea Jenkinsi (Mortin)

Rhtnoclovis pfefferi ( Dunker )

Rhmoclavis ? sp B

Clypeomorus morus (Lamarck)

"Cerithium alternatum Sowerby"

Cerithium rubus Martyn

Centhium sp E

Cerithium jonkeri Mortin

Cerithium sp C

Cerithium sp F

Cerithium sp a

SUPERFAMILY EPITONIACEA

Epiiunium scatare ( Linn )

SUPERFAMILY STROMBACEA

Diertomochilus crispatus (Sowerby)

7/f - fusus (Linn)

St- 'r-bu5 modiunensis Martin

Si -'hus pticatus pulchellus Reeve

gendinganensis Martin
fennamai ? Martin
SUPERFAMILY CYPRAEACEA
■hitiaris Gmelin"
loraria ? Linn
SUPERFAMILY NATICACEA
(Roding)
<a (Recluz)
L 'ciho papitta (Gmelin)
' :es sp. o
I ces solida (Bloinvrlle)
les aurantius (Roding)
'^ marochiensis (Gmelin)
^ cf /V columnans Reclu2

SUPERFAMILY TONNACEA
-■-I) glauca (Linn )
cohaticutata ( LInn.)
'lum bayeri Alteno
■ um gracile ? (Reeve)
sio reticulata (Rbdmg)
on bituberculans (Lomorck)

SUPERFAMILY MURICACEA

M.- -K sobrinus (A Adams)

SUPERFAMILY BUCCINACEA

Parametaria philippinarum (Reeve)
■ Hindsio acuminata (Reeve)

l^elongena gigas (Martin)

Melongena gateodes (Lomorck)

Hebra subspinoso (Lomorck)

Hebra jonkeri (Mortin)
. Nioiha sp. c( N. gemmulala (Lomorck)

UPPER CANGUINSA LATE TERTIARY MOLLUSKS, BONDOC PENINSULA, LUZON, PHILIPPINES

SYNONYMY AND IDENTIFICATION REFERENCES

LOCALITIES RANGE ILLUSTRATIONS

S £ S 5 s

TEXT -FIGURE 3, SHEET I

7-9
10-12
13,14

23,24

26,27

46,47

48,49

50,51

52,53

54,56

59,62

57,58

UNFIGURED

SHUT0p53, PI I, fig 1-3,5-7
= USNM 419513, Guimoris, Phili

EXPLANATION OF SPECIES- SYMBOLS
RARE 1-3 SPECIMENS

COMMON 4-10 SPECIMENS

ABUNDANT II OR MORE SPECIMENS
PRESENT IN EPOCH

SHUTO, p96, PI I, fig 4,8.15, MACNEIL,p 36. PI I, fig 18,22,26, UCLA 24677.41436
MACNEIL,p 38, PI l.fig 17,21.25, = USNM 229223, Linopacon SIroif, Philippines ; = UCLA 24678
TESCH 1920, p58, PI 14, fig 191, MARTIN 1891, p 220, PI SXXm. fig 509 [ = UCLA 18198, 43026
MARTIN 1891, p.2ll, PI. »»»ll fig 480,0, b

MARTIN 1879, p. 65, PI, H, fig 6; MARTIN 1891, p 216. PI :XXXIII, fig. 499,500,502. [/= tf/oc/yo/'/e/JSM:, USNM 232879, Catonduanes, Philippin
HABE 1964, p 41, PI 12, fig 19, = USNM 275856. = UCLA 31442

REEVE,C.I, Cerithium, PI, 3ZE, species 42, = USNM 243952, ^UCLA 23687

= "Centhium alternatum Sowerby", USNM 18652, Singapore; = USNM 634325, Yop, Caroline Is.

TESCH 1920, p 55. PI. EHS.fig 176-177

MARTIN 1883-87, p 148, PI. 3ZIII, fig !46; TESCH I920,p 54,Pl,l3.fig 178-9 .DICKERSON I922,PI 2,fig 9o,9b LCerithium herklotsi Y. Mortin D

KIRA 1962, p 30, PI 14, fig. 21, M4CNEIL, p44, PI.I2,fig.6; =USNM 20265, Mindanao

SHUTO, p 70, PI 3, fig 7-9,11,12.16,17; DICKERSON 1922, PI 5, fig 2 LRostellaria crispata Kiene

KIRA l962,p.35,PI I6,fig9, SHUTO, p. 71, PI 3,fig. 14,15, 18,19

MARTIN 1891, p 183, PI. 3XIX, fig 422,0, b. = USNM 622815, Zonzibor; ABBOTT, p 114

ABBOTT, p 92. PI 18, fig 3, PI 63. fig, 2

SHUTO, p 73, PI 3, fig. 1, 10, PI 4, fig. 2,3,7; = UCLA 42954,42955

MARTIN 1891, p 187, PI TTnr fig 432-433

MARTIN 1891 , p 181, PI TT!T fig 418-420

= USNM 229236, 241232, Cypraea miliaris Grr
= USNM 670719, "Cypraea parario ? Linn "

Cebu

SHUTO, p8l, PI. 5, fig 5,6,9; HABE, p 59,PI 17, fig 10; MARTIN 1891, p266, PI 3XXH, fig 642, C/Voteo me/OTOStomo Gmelin]

SHUTO, p 85, PI. 5, fig. 12,14, =UCLA 35903, " Polinices aulacaglossa Pilsbry a Vonnotto"

MARTIN 1891, p 269, PI. XL, fig. 647.64 8, TESCH 1920, p 68, PI 14, fig. 204, LSigaretusl, =UCLA 26434

= USNM 17104, "Natica marochiensis Gmelin, vor."

HABE, p 60, PI 18, fig 3, ZNatical, ? MARTIN 1891, p 259, PI VXXWMI . fig 618-620, INatica globosa Chemnitz]

SHUTO, p 83, PI 5, fig 3,4, TESCH l920,p72,PI 15, fig. 211. MARTIN 1891, p 263. PI IXZIE.fig 631, ?632

SHUTO, p77, PI 6, fig 1-4,6-9, TSP, v8,p 22, PI 5, fig 74-76,= UCLA 41732,41733

cf T8i P, v8, p 47, PI 20, fig 4

HABE 1964, p68, PI 20, fig 9; -UCLA 1490, Jopon

HABE 1964, p 76, PI. 24, fig 6

ALTENA 1942-43, p, 104, fig 2o,b

REEVE, 0 1 , Triton. PI 22, species 58; = USNM 257576. Philippines, off Tinakto Point, Towi -Towi

KIRA,p 55, PI 22, fig 10, TESCH 1915, p 69, PI 10, fig l5lo.b, iPersonay. -- UCLA 25099

MARTIN 1891. p 149. PI 3XIII, figs 349-351, C/?c7ne//(7]

KIRA, p, 57, PI, 22, fig 19; ? DICKERSON 1922, PI 4. fig, 13b, IRanelta subgronosa Beck]; "UCLA 41799

KIRA.p,63, PI 24,fig,l2;cf, SHUTO, p 104, PI. 8,fig, 4, 15, 16, [/Wi//-«a- cf M rectirostris aduncospinosus RMMi'i. ' VSNU 344150. Jopon Seos

HABE a KOSUGE 1966, p 58, PI 21, fig. 16, 17

REEVE, C I., Triton, PI XH, species 54;= USNM 669884, Keeling. Taiwan, ■ ? FISCHER, p. 64, PI 2, fig. 33o.b, C« /sjcA/ Fischer]

MARTIN 1891, p 90, PI XI5L,fig E:05,205o,b, PI ZIII,fig 204, MARTIN 1883, p. 211, PI X. fig. 12. DICKERSON 1922. PI 4, fig. II

REEVE C I , Pyrulo, PI 301, species 22.23, DICKERSON 1922, PI 2, fig 19, PI 3, fig 10, l.Pyrula'S

TESCH 1915, p56, PI. 9. fig 123

MARTIN 1883. p. 123. PI MI , fig 126, TESCH 1915. p. 57, PI. 9, fig. 124, DICKERSON 1922. PI.3. fig. 16 C/Vosso ?i/<7rf/-<7s; (Hidclgo)]

cf MARTIN 1891, pl06, PI. XSZH, fig 237,237a, C/Viresoyemmu/o/o Lamarck. var.];»UCLA Zf,i79."Niolha gruneri (Dunker)"

SPECIES

CLASS GASTROPODA

SUPERFAMILY CONACEA (coni)
ii3 Terebra duphcoto 1 Lmnaeus
114 Terebra myunformis ? Fischer

SUPERFAMILY PYRAMIDELLACEA

116 Popo sulcata (Gmelin)

CLASS BIVALVA

SUPERFAMILY NUCULANACEA

117 Yoldia Sp. a

118 YoldiO sp. $

SUPERFAMILY ARCACEA

119 Anadora pangkaensis (Morfrn)

120. Anodara antiquata ILinnoeus)

121, Anadara biformis (Martin)

122 Anadara cornea (Reeve)

123 Anadara granosa (Lmn)
124. Anadara sp a

125 Trisidos semitorta (Lomarckl

126 Sfr/arco o/ivocea (Reeve)

127 "Stnarco sinensis" Hobe 9 Kosuge, non Thiele

SUPERFAMILY LIMOPSACEA

128 Limopsis sp $

129 Clycymeris sp. a

130 Glycymeris sp A

131 Glycymeris sp. B

SUPERFAMILY PECTINACEA

132 Amussium pleuronectes ? (Linnaeus)

133 Chlomys crossicostotus ? (Sowerby)

SUPERFAMILY LUCINACEA

134 Cyci'-'cama oblongo (Sowerby)

SUPERFAMILY CARDITACEA

135 Card -j canaliculafa Reeve

SUPERFAMILY CARDIACEA

136 LoB'. :rdium cf L multipunctatum (Sowerby)

137 iofi rdium unicolor ? (Sowerby)

SUPERFAMILY TELLINACEA

rdia off M ifulgar/s iReeve)

SUPERFAMILY VENERACEA

erycma (Linnoeus)
sinensis ? (Gmelin)
■fio papyracea Gray
•iuglypta 1 (Philippi)

■--r. isabellina (Philippi)

SUPERFAMILY MYACEA

'rttsulcafa Smith
meliata Fischer
uophoides" le%tt\,non Hinds

UPPER CANGUINSA LATE TERTIARY MOLLUSKS. BONDOC PENINSULA, LUZON, PHILIPPINES

SYNONYMY AND IDENTIFICATION REFERENCES
PLATE FIGS

LOCALITIES RANGE ILLUSTRATIONS

. S S g i I 5 "

TEXT-FIGURE3, SHEET 3

160,161
157-159

174-176
177,180

190-192
193-195
I96-I9B

SHUTO,p-23l, PI 23,fig 4,Ov/ome/-//i7, REEVE, C I , Terebro,P\ I, species 3
FISCHER, p, 89, PI. 3, fig. 67a, b, off USNM 343418, "7/jAe//oso Reeve, Kii, Japan"

HABE in KURODA, 1949-53, p,4l, Text-fig liREEVE,C, 1, 7o/-n(7/e//o, PI I, species 4; OICKERSON 1922, PI, 2,fi9 2,C/lc/oeo/) re//ci//i7/i/s K Mottin:

JSNM 204406,

on in Japan seos, Yesso, Hondo, Kagoshima Gulf

MARTIN 1891, p 372, PI Lni,fig- Il7a, b, c

MARTIN l89l,p37l,PI Ln,fig 96, [/1/-CO femomo/Ji VANDERVLERK,p 289, note 19; =USNM 631801, Cebu,Philippin

MARTIN 1891, p 377, PI LIE.fiq 113,114, TESCH 1920, p 94, PI 20, fig. 253,254, FISCHER, p 118

MARTIN 1891, p 379, PI LBZ, fig, 118- 120; TESCH 1920. p, 96, PI 20,fig 256, REEVE, C.l.,/3/-<ro, PI 3, species 16

TESCH I920,p 92, PI 19, fig, 248, 249; MARTIN l88l,p-242; ? DICKERSON 1922, PI 6, fig, 4

KIRA.p, 123, PI, 44, fig. 3; REEVE, C, I, <3/-i:o, PI UK, species 89

REEVE.C. l.,/3reo,PI,S2r, species 113

HABE a KOSUGE I966,p, 126, Pl,47,fig, l,?non THIELE 1931, p 174, PI, I. fig, 7

= USNM 294954, off Marinduque, Philippines

cf UCLA 50070, Glycymeris modesta (Angos), New Zeolond

? REEVE, C I , Pecten, PI XE, species 48, ? ' USNM 258262

REEVE, C I , Pecten, PI will species 64,= USNM 333860, Chlamys crassicostolus (Sowerby)

REEVE, C l,Co/-o'(/o,PI3nn:,species40; DICKERSON 1922, Pi (,.f\q.lQ,lC anhquata Linn :,?FISCHER,p,l2l,PI 5, fig, 109, "CyOKOno Moftin

cf UCLA ^Q71B"Laevtcordium multipunctatum (Sowerby)"; DICKERSON l922,PI,6,fig,7, CCffrtf/i/m elongotum (Bruguiere)3
REEVE,C.l, Cardium, PI lEDI, species 86, DICKERSON 1922, PI, 6. fig. Bo, 8b "Card/um unico/or (Sovwerby)"

HABE a KOSUGE,p 162, PI 63, fig 16; DICKERSON 1922, PI 6.lig.9<i.9b,Cardnim donaciformis Cuming, USNM 248123, Bohol, Philippines

cf REEVE, CI,, Isocardia, PI I, species ZAsocardia vulgaris

? HABE a KOSUGE, p \6A,P\ d'^Jiq.S.Coslacallisto erycino (Linnoeus), = UCLA 24100 a 26270

KIRA.p I59,PI 57,fig 5

HABE,p,l93,PI,59,fig,l9, = USNM 297653, Borneo, off Sondokon Islond

KIRA.p 161, PI 57,fig,25

HABE a KOSUGE, p 160, PI 63, tig 4; cf TESCH 1920, p 104, PI 2 1, tig 275a,b, CHenus chlorolica Philippi]; UCLA 50818

SMITH 1878,p,819,PI, L.fig 23,23o,23b;HABE,p, 204, PI, 63, fig, 6; DICKERSON 1922, PI, 6, fig, l3a,l3b,C(ro/'ii/to scaphoides K\ni%1
FISCHER, p, 131, PI 6, fig 124-126, off, Annocorbuln scophoides Hinds, in HABE 8 KURODA, p 3, PI, I, fig 13,14
TESCH, p 106, PI 22, fig, 281-283 non C scaphoides Hinds, REEVE, C I, . Coz-Au/o, PI, 3, species 24

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

Text-Figure 4. Species - Range Diagram, Upper Canguinsa Molluscan Fauna, Philippines

Locality 2x -1388 Locality 3x Locality llx

L.Mio.

U Mio

PIlO.

Pleis

Rec. 1

^/////1(2*1V///I 1

90-
o

1(2%) -

-r :::::////// \

•^80-
o

yyyy// 9 ( 1 6 % l//^'/^^^

c 70-

m///M

leo-

6(9%),

g 50-

/////////

////

^40-

/yZ^8J32%

1^0-

//?(4

xy//

£20-
(J

ID -

J5R4%J

n —

1 1 1

^VZ

Species in touna

Species m fauna

Species in fauna

Gastropods

Bivalves

Recognized species 58

Recent species 50

% Recent sp. m total fauna 78%
%Recent sp in recognized
fauna 86%

Recognized species 49

Recent species 40

%Recent spin total fauna 71%
% Recent sp in recognized
fauna 82%

Recognized species 48

Recent species 43

%Recent sp m total fauna 75%
% Recent sp in recognized
fauna 90%

long as geologic ranges of the unidentified forms
are unknown. Therefore, the proportion of Re-
cent species is represented by a double per-
centage figure as explained above. The true per-
centage then lies somewhere between the two
given, and for reasons given above, probably is
nearer the minimum than the maximum. Per-
centages for all localities on this calculation are
given below:

2X-1388 78%-89%

3X 73%-86%

4X 81%-85%

IIX 157c^9\%

1389 78%-89%

1390 77%-85%

Martin, Tesch, Fischer, Shuto, Oostingh and
a few others have rather consistently placed in
the Pliocene fairly large faunas having from 50%
to 64% Recent species. In a few instances (Oos-
tingh 1935: 222; Fischer 1927), faunas with

slightly under 50% Recent species have been
considered Pliocene. Records of Quaternary
faunas are few. Martin (1883-87: 348) lists only
two for which percentage figures are given,
"Umgegend von Grissee," with 30 mollusca,
90% Recent species, and "Untergrund von Ba-
tavia, bis 6 m. Tiefe," with 22 species of which
86% are Recent. Thus, percentagewise, there is
a considerable interval, 65% to 86%, that is rep-
resented by no sizable fauna. It is in this interval
that the Bondoc Peninsula faunas appear to be-
long. On this basis they may be dated as very
late Pliocene or very early Quaternary.

Other data suggesting that the Bondoc Pen-
insula faunas are of Pliocene age have been men-
tioned above where it is shown that from 54%
to 72% of the species from the several localities
are known elsewhere from Pliocene, but not
from earlier beds. This strongly Pliocene aspect
of the faunas is tremendously increased if we
disregard the species for which no other occur-

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

rence is known, and those which are elsewhere
known only in the Holocene. For example, lo-
cality 1 IX. which has 57 recognized species, has
only 32 identified species with occurrence in the
fossil record: 30 of these occur in the Pliocene,
but only 17 are found in Miocene strata, and
only I species, doubtfully determined, is con-
fined to the Miocene.

In summary, the Canguinsa molluscan faunas
are probably late Pliocene or possibly early
Pleistocene in age. in the sense that these terms
are used by western Pacific molluscan paleon-
tologists. The conclusion of Dickerson that Mio-
cene faunas of this region contain 75% Recent
species is therefore without basis.

The much more difficult problem as to the dif-
ferent rate of evolution of molluscan faunas in
the tropics as compared to temperate seas can-
not be confidently solved at this time, but some
facets of the problem are considered next.

Rates of Evolution. — The term "rates of evo-
lution"" as used by Dickerson evidently applies
to what might be termed differences in percent-
age of Recent (or extinct) species between con-
temporary tropical and temperate faunas. The
arguments put forward to explain these differ-
ences are based upon inferences and conclu-
sions that do not appear valid at this time. Dick-
erson's conclusions depended upon his dating of
the Canguinsa molluscan fauna as Miocene,
whereas work subsequent to publication of his
conclusions suggests that the Canguinsa fauna
is much younger.

The concept that tropical later Tertiary faunas
contain a higher percentage of Recent species
than do contemporary temperate or arctic fau-
nas apparently was first put forward by Martin
(1879-1880: 22-30), and it is here that Dickerson
may have found the germ of his conclusions re-
garding the Canguinsa fauna. Martin (op. cit.:
29) states that the true percentage of Recent spe-
cies in the Javanese faunas described was prob-
ably near 50%, approximately the percentage of
the lower Pliocene of Europe. Martin's Javanese
faunas closely resembled those described a little
earlier by Medlicott and Blanford (1879) from
the Gaj Series of Sindh and referred by them to
the Miocene. As the Javanese faunas showed
little or no resemblances to Eocene faunas and
little or none to (known ?) Pliocene faunas, Mar-
tin concluded that they, too, are probably of
Miocene age. Martin (op. cit.: 22-24) discussed
at length the difficulties attendant upon corre-

lating tropical Indo-Pacific faunas with contem-
porary assemblages in Europe, summarizing
these difficulties as follows (free translation by
us): "However, neither the species which are
related to or are identical with European ones,
nor even the percentages of Recent species
found in [European] Tertiary beds supply a
ways-and-means for the age determination of
tropical Tertiary beds.""

Martin explained this situation in paragraphs
a little too long to quote, but which he summa-
rized forty years later (Martin 1921: 763: trans-
lation by T. Wayland Vaughn):

That I designate as Miocene, sediments which contain
45% of hving molUisks. may raise doubt, especially when
this estimated percentage, for reasons already stated, is
appreciably below the real percentage. In reply to this, it
is to be emphasized that in similar Neogene sediments of
Europe and the Indies the deposits in the latter region must
contain a higher percentage of living species than the for-
mer [Martin's italics). This is because there was during the
Tertiary time important climatic changes in the extratrop-
ical regions while no such changes took place in the tropics.
In the tropics, accordingly, there were fewer factors which
would modify the species and. therefore, the transforma-
tion of the fauna in the tropics did not take place so rapidly
as in our [European] region and. consequently, more spe-
cies have persisted until present time. The younger the stra-
ta are, the larger must be the differences in percentage for
equivalent strata in Europe and the Indies; precise values
for these cannot be given.

The two concluding sentences in the para-
graph quoted above are of particular interest.
The statements seem untenable, and it is hard
to avoid the feeling that they imply interpreta-
tions that the author did not intend to put for-
ward. If accepted at face value, the implication
is that in Miocene times tropical faunas will have
a higher percentage of still-living species than
do contemporary Temperate-Zone faunas; in Pli-
ocene time the disparity in percentage between
the faunas of the two regions increases and. by
inference, would necessarily be progressively
yet greater in the Pleistocene and Holocene ep-
ochs. Stating the situation somewhat differently,
the Recent faunas of the Indo- Pacific region con-
tain a higher percentage of living species than
do the Recent faunas of the European coasts. If
it be argued that Martin's statement applies only
to later Tertiary faunas, the same absurdity
holds, for every time-horizon in the later Ter-
tiary— lower Miocene, upper Miocene, Pli-
ocene— had its then-living or "Recent"" faunas
which, it is implied, differed in percentage of
"Recent"" species in Indonesia and in Europe.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

The hypothesis presented above is that of a
very able worker with profound acquaintance
with Indonesian later Tertiary faunas, but it re-
mains only an hypothesis and has not been sup-
ported by later work. Indeed, a small amount of
evidence brought out in the last half century
tends to throw doubt on some of the basics of
this hypothesis.

It is clear that Martin's ideas regarding the
fundamental differences in percentage of Recent
species in late Tertiary tropical faunas, on the
one hand, and those of temperate and cold seas,
on the other, cannot be tested until it is possible
to correlate with considerable refinement across
these latitudinal barriers and, in this case, par-
ticularly between tropical Indo-Pacific and tem-
perate west European faunas. Unless we know
with a considerable degree of precision that two
faunas are of the same age. we have no basis for
evaluating any differences they may show in
percentage of Recent species. Quotations from
two active current workers in this field suffice
to show that the problem of interprovincial cor-
relation still escapes solution. Cloud (1956: 560)
wrote: "Establishment of age equivalents in the
standard European succession is perhaps the
most difficult task of Indo-Pacific Cenozoic cor-
relation. Indeed it is sometimes considered im-
possible, and efforts to do so are periodically
abandoned." H. S. Ladd (1966: 9) stated: "Age
determinations and correlations involving major
stratigraphic units in the several island groups
are based on the letter classification established
for Indonesia. No attempt is made to tie these
Indonesian units to the stages of the standard
European sequences. Efforts of this sort have
been made, but most such efforts have been re-
garded as tentative, even by their proposers."

The factors inferred by Martin to be respon-
sible for the differing rates of faunal change are
those of the physical environment. He believed
that temperature changes were minimal in the
tropics throughout later Tertiary time, whereas,
in the later Tertiary European seas, a steady
decline in marine temperatures obtained, cul-
minating in the glacial climates of the Pleisto-
cene. He believed that factors other than that of
marine temperature were operative with about
equal intensity over both time and space. The
nearly persistent warm seas of the tropics ex-
erted little influence productive of faunal
changes, hence a greater percentage of the fau-
nas in any time-horizon persisted into later times

and ultimately into the Holocene. In line with
the above inferences. Martin used a percentage
scale for the Indonesian Tertiary differing con-
siderably from that used by western European
and western Atlantic paleontologists. Compari-
son of these scales is given below:

European

AND

Eastern

Indo-

American

nesian

Epoch

(%)

Pleistocene

+ 50-100

70-100

Pliocene

30-50+

50-70

Young Miocene
Old Miocene

}

3-30

20-50
8-20

Since Martin's (1919) summary, a number of
comprehensive studies of Indonesian later Ter-
tiary faunas have appeared. In these, there is a
tendency to consider as Pliocene, faunas with
percentages of Recent species somewhat lower
than those given above as the lower limit for this
epoch. Thus, Fischer (1927: 11) placed the fau-
nas of the Fufa Beds of Seran and Obi in the
Pliocene with 46.8% Recent species. Tesch
(1920: 110 et seq.) included in the Pliocene of
Timor assemblages containing as low as 43%
Recent species. Oostingh (1935: 222 et seq.).
using Martin's methods, considered his Pliocene
Kali Bieok Beds to be older Pliocene; on the
basis of superposition, he considered them older
than Martin's reference fauna for the Pliocene —
the Sonde Beds, with about 53% Recent species.

If. as has been implied, uniformity of the trop-
ical climates has resulted in slow faunal altera-
tion, whereas the changing climates of higher
latitudes have accelerated faunal change, the
tropical later Tertiary faunas of the New World
should show relatively high percentages of Re-
cent species, as has been claimed for the Indo-
nesian faunas. In the last half century, a number
of extended studies on tropical American Neo-
gene faunas have appeared, including works by
Woodring (1925, 1928), Weisbord (1929, 1962,
1964). Olsson (1922), Pilsbry and Olsson (1941),
Jung (1965, 1969). Marks (1951), Maury (1934),
and others. The faunas considered in these stud-
ies have commonly been dated according to the
percentage of Recent species recognized or by
comparison with earlier described faunas which
have themselves been dated by the percentage
method. The scale used is approximately that

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

used by European and American workers (as
given above), and which also approximates the
percentages used by Lyell (see Davies 1934: 56-
57). Woodring (1928: 107). and Vaughan (1923:
526). Roughly, large faunas with Recent-species
percentages between 3% and 30% would be
placed in an appropriate part of the Miocene;
those with Recent-species percentages of 30%
to 509f would be considered Pliocene. These
percentages, at least for middle Miocene and
younger, are 10-20% below those given for
"Miocene" and "Pliocene" faunas of Indonesia
by Martin. The faunas considered above are all
tropical; therefore, these differences in percent-
ages can scarcely be due to differences in marine
climate. They suggest, for example, that the
"Pliocene" of Indonesia may well represent a
time interval different from, and quite possibly
somewhat younger than, that of the "Pliocene"
of tropical America, or that influences not yet
recognized are responsible for the discordance
in percentages.

A recent work on the Caloosahatchee fauna
of southwestern Florida (Du Bar 1958) adds to
the anomalous situation discussed above. This
Caloosahatchee fauna is very large and has uni-
formly been considered tropical (Dall 1903:
1605; Du Bar 1958: 88). The calculated percent-
age of Recent species in the assemblage varies
considerably with the individuals who have ana-
lyzed it. emphasizing, perhaps, the importance
of the personal factor in specific determinations.
Dall ( 1903: 1604) determined 639 moUuscan spe-
cies of which 48% are Recent; Olsson and Har-
bison (1953: 10) recognized 505 species of which
33.8% are Recent; while Du Bar identified from
the type-locality 341 species of which 39.5% are
Recent. Diverse as these figures are. they would
all date the Caloosahatchee Beds as later Mio-
cene if the yardstick used by Martin were ap-
plied, and as Pliocene according to the scale
used by most students of the American later
Tertiary. However. Du Bar (1958: 138-139) col-
lected in place in the Caloosahatchee Beds a
small mammalian fauna, including horse teeth
identified as Equiis sp. cf. E. (E.)lcidyi from two
different levels. This genus of horse is common-
ly thought to be restricted to Pleistocene and
Holocene time. Thus, the Caloosahatchee fauna
would, by some, be placed in the Pleistocene,
despite having between 33.8% and 48% Recent
species of MoUusca.

In summary, the Canguinsa molluscan faunas

are probably late Pliocene or possibly early
Pleistocene in age. in the sense that these terms
are used by western Pacific molluscan paleon-
tologists. The conclusion of Dickerson that Mio-
cene faunas of this region contain 75% Recent
species is therefore without basis.

ACKNOWLEDGMENTS

The study described in this paper would have
been well-nigh impossible without the generous
aid of a number of colleagues and museums who
have put their facilities and knowledge at our
disposal. Loan of Dickerson's original collec-
tions was made by the California Academy of
Sciences through the authority of its curators in
the Department of Geology, the late Drs. G.
Dallas Hanna and Leo G. Hertlein. and its pres-
ent curator of Geology. Dr. Peter Rodda. Simi-
larly. Dr. J. Wyatt Durham and Mr. Joseph
Peck, of the Museum of Paleontology. Berkeley,
have loaned us Dickerson's large original col-
lection from locality llx. We have been given
full access to the fine reference collections of
Recent shells at the above institutions, at the
United States National Museum of Natural His-
tory, and at the University of California at Los
Angeles. Dr. A. Myra Keen of Stanford Uni-
versity has aided in the identification of a num-
ber of rare South Pacific gastropod species; Mrs.
Jean Cate and Dr. Walter Cernohorsky have
kindly identified the miters. The superb photo-
graphs of the fossil specimens illustrated were
taken by Mr. Takeo Susuki of U.C.L.A. The
exacting preparation of the faunal range and dis-
tribution charts is the work of Miss Julie
Guenther. Finally, all phases of the work upon
the molluscan faunas have been greatly im-
proved by the cheerful, informed and patient aid
of LouElla R. Saul.

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(Geol.). 11:137-190. pis. 15-27. 1 table.
Zeigler. R. F.. and H. C. Porreca. 1969. Olive shells of

the world. Zeigler & Porreca. % pp.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA 33

APPENDIX A— NOTES

1. See Kleinpell (1958: 4-5. footnote 3. and p. 7. footnote 4) for the nature and the fate of the
fossils upon which these discussions were originally based. It had been the hope and plan of
the writers in 1941 that the late Frank Merchant, who had assisted them in these studies, both
in field and laboratory, and with particular emphasis upon the mollusk collections, would, with
the fellowship that had been granted him at the California Institute of Technology, be able to
pursue these studies to their logical conclusion. But at that point the second World War inter-
vened. Mr. Merchant's promising career was violently terminated in a war-time prison camp.
At the Bureau of Science in Manila. 18 large cabinets containing thousands of specimens of
some seventeen hundred mollusk species, along with the microscopic slides of foraminifer
types, assemblages, and polished limestone sections also stored there, were totally destroyed
in the shelling during the American recapture of Manila. Subsequently, cloth-sacked foraminifer
samples stored in a company riverside bodega, surviving the hostilities, disintegrated into
incoherent mud and rot for lack of post-war curatorial funds. By 1951. nevertheless, four
volumes of the nine comprising the Philippine Petroleum Survey's preliminary report, preserved
in the States, had been published, salvaging much of the data and preliminary conclusions.
Unhappily for the paleontologic checklists, however, the aims of the preliminary typology and
distributional data (see Corby etal. 1951: 231. 292-297) which they record were totally defeated:
even descriptions of the fossil localities to which they are geared were not included in the
partially published report, though these may be found in copies of the original report on deposit
in the Manila Bureau of Mines, and some of them do appear, graphically located by numbers,
in some of the areal geology maps included in the publication. Too. a handful of duplicate
specimens and slides, although scattered, had been preserved outside the war-devastated area
through the foresight of the late Dr. Quirico Abadilla. Director at the time of the Philippine
Bureau of Mines, who also lost his life in the final phases of the hostilities. Through the
assistance of the post-war Philippine Bureau of Mines, Mr. Earl Irving and associates of the
U.S. Geological Survey, and the management and staff of the Philippine Oil Development
Company, considerable recollecting of fossils has been made possible (although, unlike neon-
tological specimens, fossils do not reproduce their kind). Thus, it has been possible to reas-
semble at least some of the more critical material, either in original or duplicate form, over the
years. In addition, the senior author has been able to study the original Dickerson molluscan
material on deposit at the California Academy of Sciences and in the Museum of Paleontology
at the University of California in Berkeley.

2. See Kleinpell (1958: 1-3). Comparison with material in Bandoeng. Java, and Balikpapan. Bor-
neo, had been projected and. in fact, subsequently accomplished, after preparation of the
Petroleum Survey's preliminary report. The biostratigraphic sequences selected to typify the
tentative local age classification have retained descriptive value as presented in plates 34, 40.
and 42 of the Corby et al. (1951) report. Especially valuable in this connection are plates 31
and 43 and the accompanying discussion of Philippine larger foraminifers (pp. 247-250. 264-
288) by Morrison et al.

3. This PODCO report on the reconnaissance geology and oil possibilities of northern Luzon was
at that time made available, along with the paleontological data from the localities published
by Corby et al. ( 1951: pi. 10). to the geological staffs of American Overseas Petroleum Limited
(see Durkee and Pederson 1961: pi. 137) and STANVAC. who were subsequently engaged with
PODCO in joint geological exploration of the Cagayan Valley. Further studies, with the same
context, were pursued in conjunction with Paul H. Dudley. Benjamin Daleon. and Mario Nieto,
and references to scientific aspects of these private data were released for publication as of
January 1957 (see Kleinpell 1958: I. footnote 2).

4. This Tuguegarao Sandstone, essentially non-existent as a formational unit, was nicknamed by
the field party at that time the "Kamlon Formation" after Datu Kamlon of Jolo who. up until
that time, had successfully eluded every attempt by the Philippine army to find and capture
him.

34 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

5. See Corby et al. (1951: pis. 34 & 35). Here the highest orbitoids occur in sample P-JH 32 within
the "Type Upper X'" portion ot the sequence along the "Tarao" (a cartographer's misspelling
ot the original Jarao) River, the lowest "Rotalias" of the species in reference {"Rotalia'^ sp.
1. sp. 2. and sp. 3) in sample P-JH 15 of the "Type Y" part of the same sequence, and
extending upward in greater abundance stratigraphically higher in the "Type Y" and through
the "Type Lower Z" sequence.

6. See Corby et al. (1951: pi. 40). Here the highest orbitoids ("Tryhliolcpidcna^" sp. 35 and sp.
36, including "T." rutteni. and Miogypsina) occur in the sampled sequence C-JH 38-0, 39-0.
and 40-0 near Sibonga, and C-JH-37B-0 on the Aloguinsan-Barili road near kilometer 78, all
in the Lower Limestone Member of the Barili Formation; and in the overlying marls and
limestones the "Rotalias" in reference are far rarer than in the more clastic facies of the
Philippine Neogene.

7. See Corby et al. (1951: pi. 31). Here the highest orbitoids are again of f3 age. from localities
155 and 156, as reported by Yabe and Hanzawa. the "Rotalias" are rare and restricted to the
higher Hubay Formation and associated with its molluscan faunas.

8. Through permission from Colonel A. Soriano and the Philippine Oil Development Company to
include references to private data in notes for publication. See Kleinpell (1958: 1).

9. Thus, the former Lubuagan "coal measures" or Lubuagan Formation on the west side of the
valley became, in effect, the Mabaca River Group with three formations (a lower Asiga. a
middle Balbalan Sandstone, and an upper Baluan). On the east side it became the Gatangan
Creek Formation; the former Callao Limestone along the northwestern edge of the valley
became the Sicalao Limestone, a name extended to also include the former Ibulao Limestone
of the Kiangan syncline in Ifugao and that of the south end of the valley (southwest of Mones.
Isabela). while the name Callao was restricted to the original typical area along the eastern
side. The former lower mudstone member of the Ilagan Formation along the east side became
the Baliway Formation, following the designation of Vergara et al. (1959: 47. 52); the term
Ilagan Formation was restricted to the upper more preponderantly coarse-clastic member of
that formation in previous usage; and the designation Lallo Formation, without a type section
due to poor exposures, was applied to the more or less tuffaceous elastics of variable texture
previously mapped for the most part as Ilagan in the Apairi basin of the extreme north. Certain
distinctively thin-bedded limestones in a relatively small and isolated area in the north became
the Abaan Limestone, and the term Awidon Mesa Formation was given to certain welded tuffs
and pyroclastics of Lubuagan.

10. See Corby et al. 1951. plate 10, localities LHB-301, 303. 306. 494. 726. 365. 461. 462. 469. 470,
471, 472, 473, 475, with Eulepidina . Miogypsina . and associated small foraminifers. all of
Tertiary e age. and localities LHB^96. 497. 701. 796. 463. 464. 465. 480. 481, 487 and, espe-
cially, 474. 482. 483. 484. 488 and 489. all with Tertiary fl orbitoids. as at LHB-315 near the
top of the Sicalao, or former Callao Limestone, extension farther north in the area southwest
of Luna.

11. See Corby et al. 1951. plate 10. localities LHB-727. 558. 560 and 562.

12. Localities D-1581 (LWP-35). D-1583 (LWP-33). D-1586 (LWP-29). D-1587 (LWP-28). D-
1589 (LWP-24). D-1594 (LWP-19) and D-1597 (LWP-1 = Dickerson's locality 2x). The last-
mentioned locality is especially rich in "/?<>/fl//V/" heccarii koehoecnsis LeRoy; "Rotalia"
indopacifica Thalmann. "Rottdia" japonica Hada. and "Rotalia" ketienziensis (Ishizaki) are
well represented; and "Rotalia" papillosa Brady is especially abundant in samples LWP-19.
24. 28 and 33.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA 35

APPENDIX B— REGISTER OF CIT FOSSIL LOCALITIES,
BONDOC PENINSULA. LUZON. PHILIPPINES

1388 CIT Blue-gray sandy marls cropping out on right bank of Bahay River. 1219 m (4000 ft) S

25°E of the mouth of Apad Creek, and about 366 m ( 1200 ft) upstream from abandoned
oil well on left bank of river (Dickerson's Bureau of Lands bench mark no. 1). Bondoc
Peninsula. Tayabas Province. Same as locality 2x/RED. 27 Nov. 1937. Collectors: W.
P. Popenoe, Peregrino Romania and Cosme Albis.

1389 CIT Gritty sandstones in bed of Bahay River. 152 m (500 ft) N 40°E of the mouth of Apad

Creek. Bondoc Peninsula. Tayabas Province. Same as locality 5x RED. 27 Nov. 1937.
Collectors: Popenoe. Pomania and Albis.

1390 CIT Soft blue sandy marls cropping out in bed of Bahay River, about 488 m( 1600 ft) upstream

from abandoned oil well (Dickerson's Bureau of Lands bench mark no. 1). Bondoc
Peninsula. Tayabas Province. 27 Nov. 1937. Collectors: Popenoe. Pomania and Albis.

Descriptions of RED localities 2x, 3x, 4x, 5x and I Ix are recorded on p. 4 of this paper.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA 37

PLATES
ILLUSTRATIONS OF CANGUINSA FOSSIL MOLLUSKS

We have described no new species in this paper. Species names followed by nov. spec.
(=n. sp. = new species) refer to new species described by Martin in references 1879-
1880, 1881-1884. and 1883-1887. The illustrations of these species on our plates 17 and 18
are photo copies of Martin's original figures. Quotation marks enclosing specific identifi-
cations by Dickerson on plates 17 and 18 indicate dubious or wrong identification, generally
the latter.

Explanation of specimen catalogue number symbols

UCB — University of California, Berkeley, Invertebrate Paleontology catalogue
CAS — California Academy of Science, Invertebrate Paleontology catalogue
UCLA — University of California, Los Angeles, Invertebrate Paleontology catalogue

38 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 1

Figs. 1-3. Uinhoniiim vestiariiiin (Linnaeus). UCLA cat. no. 48534; Locality no. 1388

CIT; (1) apertural vieu; (2) umbilical view; (3) apical view; all x2; height 6.8 mm;

diameter 19.4 mm.
Figs. 4. 6. Neritina cf. N. donovana Recluz. UCLA cat. no. 48355; Loc. no. 1388 CIT;

(4) apertural view; (6) abapertural view; all x2; height 13.0 mm; diameter 12.9 mm.
Fig. 5. Rissoina sp. UCLA cat. no. 48356; Loc. no. 1388 CIT; apertural view; x3; height

8.6 mm; diameter 3.3 mm.
Figs. 7-9. Architectonica pcrspectiva (Linnaeus). UCLA cat. no. 48357; Loc. no. 1388

CIT; (7) apical view; (8) umbilical view; (9) apertural view; all x2; height 10.0 mm.

diameter 20.6 mm.
Figs. 10-12. Architectonica maxima (Philippi). UCLA cat. no. 48358; Loc. no. 1390 CIT;

(10) apical view; (11) umbilical viev\; (12) apertural view, all x2; height 12.4 mm;

diameter 27.3 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

40 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 2

Fig. 13. Ti'lescopinm telescopiitm ? (Linnaeus). UCLA cat. no. 48359; loc. no. 1389 CIT;
apertural view. x2; height 22.0 mm; diameter 14.2 mm.

Fig. 14. Telescopium telescopium ? (Linnaeus). CAS cat. no. 53504; loc. no. 3x RED;
apertural view. x2; height 21.0 mm; diameter 19.2 mm.

Fig. 15. Potamides sucaradjanus Martin. UCLA cat. no. 48360; loc. no. 1389 CIT; aper-
tural view, x2; height 24.8 mm; diameter 7.4 mm.

Fig. 16 ''Potamides" sp. /3. UCLA cat. no. 48361; loc. no. 1389 CIT; apertural view.
x2; height 52.9 mm; diameter 19.4.

Fig. 17. Ccrithidea ? sp. UCB cat. no. 10871; loc. no. llx RED; abapertural view, x2;
height 24.0 mm; diameter 9.0 mm.

Fig. 18. Ccrithidea jenkinsi Martin. UCLA cat. no. 48362; loc. no. 1388 CIT; apertural
view, x2; height 26.1 mm, diameter 9.5 mm.

Fig. 19. Rhinodavis pfeffcri Dunker. UCLA cat. no. 48363; loc. no. 1388 CIT; apertural
view. x2; height 16.5 mm; diameter 5.5 mm.

Fig. 20. Rhinodavis ? sp. B. CAS cat. no. 53505; loc. no. 3x RED; apertural view. x2;
height 23.9 mm; diameter 13.7 mm.

Fig. 21. Clypcomorus morns (Lamarck). UCLA cat. no. 48364; loc. no. 1388 CIT; aper-
tural view. x2; height 16.7 mm; diameter 9.1 mm.

Fig. 22. "Cerithiiim alternatnm Sowerby." CAS cat. no. 53506; loc. no. 3x RED; aper-
tural view. x2; height 12.0 mm; diameter 7.3 mm.

Fig. 23. Cerithium rubiis Martyn. CAS cat. no. 53507; loc. no. 3x RED; apertural view.
x2; height 20.0 mm; diameter 1 1.5 mm.

Fig. 24. Cerithium ruhus Martyn. UCLA cat. no. 48365; loc. no. 1388 CIT; apertural
view, x2; height 27.0 mm; diameter 10.3 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

i^Oi

>*^

j»

42 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 3

Fig. 25. Cerlthium sp. E. CAS cat. no. 53508; loc. no. 3x RED; apertural view. x2;

height 19.9 mm; diameter 8.6 mm.
Figs. 26, 27. Cerithium jonkeh Martin. CAS no. 53509; loc. no. 3x RED; (26) apertural

view; (27) abapertural view; both x2; height 40.7 mm; diameter 15.0 mm.
Fig. 28. Cerithium sp. C. CAS cat. no. 53510; loc. no. 3x RED; apertural view, x2;

height 17.5 mm; diameter 6.8 mm.
Fig. 29. Cerithium sp. F. CAS cat. no. 53511; loc. no. 3x RED; apertural view, x2;

height 14.5 mm; diameter 9.6 mm.
Fig. 30. Cerithium sp. a. CAS cat. no. 53529; loc. no. 2x RED; apertural view, x2;

height 19.9 mm; diameter 8.8 mm.
Fig. 3 1 . Epitonium scalare (Linnaeus). UCLA cat. no. 48366; loc. no. 1390 CIT; apertural

view X !; height 22.0 mm; diameter 16.0 mm.
Figs. 32, 33. Dientomochihts crispatus (Sowerby). UCLA cat. no. 48367; loc. no. 1388

CIT; (32) apertural view; (33) abapertural view, both x2; height 19.9 mm; diameter

10.2 mm.
Fig. 34. Strombus madiunensis Martin. CAS cat. no. 53540; loc. no. 4x, RED; abaper-
tural view, X I; height 37.3 mm; diameter 17.5 mm.
Fig. 35. Strombus plicatus pulcheUus Reeve. UCB cat. no. 10872; loc. no. llx RED;

abapertural view, x 1; height 37.3 mm; diameter 23.8 mm.
Fig. 36. Strombus gendinganensis Martin. CAS cat. no. 53512; loc. no. 3x RED; aper-
tural view, x2; height 27.3 mm; diameter 1 1.9 mm.
Fig. 37. Tibia fusus (Linnaeus). UCB cat. no. 10873; loc. no. llx RED; apertural view,

X 1 ; height 1 10.9 mm; diameter 30.8 mm.
Fig. 38. Strombus camirium Linnaeus. UCLA cat. no. 48368; loc. no. 1388 CIT; apertural

view, X 1; height 48.8 mm; diameter 31.4 mm.

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44 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

Plate 4

Figs. 39-42. Strombus fenmimai ? Martin. UCB cat. no. 10874. for figs. 39. 42; UCB

cat. no. 10875 for fig. 40. 41; locality 1 Ix RED; (39) and (41), abapertural view, (40)

and (42), apertural view, all x 1; no. 40, height, 41.6 mm; diameter 22.0 mm; no. 39.

42 height 32.0 mm; diameter 20.5 mm.
Figs. 43. 44. Cypmea miliaris Gmelin. UCB cat. no. 10876; loc. no. llx RED; (43)

apertural view, (44) abapertural view; x 1; height 29.8 mm; diameter 18.0 mm.
Fig. 45. Cypraea poraria ? Linnaeus. UCLA cat. no. 48369; loc. no. 1390 CIT; apertural

view. X 1; height 20.4 mm; diameter 13.5 mm.
Figs. 46, 47. Mamilla mammata (Roding). UCLA cat. no. 48370; loc. no. 1388 CIT; (46)

apertural view, (47) abapertural view, x2; height 19.5 mm; diameter 17.2 mm.
Figs. 48, 49. Neverita pctiveiiana (Recluz 1855). UCLA cat. no. 48371; loc. no. 1389

CIT; (48) abapertural view, (49) umbilical view, x3; height 15.9 mm; diameter 15.0

mm.
Figs. 50, 51. Eunciticina papilla (Gmelin). CAS cat. no. 53530; loc. no. 2x RED; (50)

apertural view. (51) abapertural view, x2; height 10.0 mm; diameter 9.7 mm.
Figs. 52, 53. Poliniccs sp. a. UCLA cat. no. 48372; loc. no. 1388 CIT; (52) apertural

view, (53) apical view, x2; height 14.9 mm; diameter 11.5 mm.
Figs. 54. 56. Polinices solida Blainville. UCLA cat. no. 48373; loc. no. 1388 CIT; (54)

apertural view, (56) apical view, x2; height 11.3 mm; diameter 10.8 mm.
Fig. 55. Polinices aurantius Roding. UCLA cat. no. 48374; loc. no. 1388 CIT; apertural

view, x 1; height 27.9 mm; diameter 21.2 mm.

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46 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 5
Figs. 57. 58. Natico cf. N. cohunmins Recluz. CAS cat. no. 53531; loc. no. 2x RED:

(57) abapertural view: (58) umbilical view. x2: height 14.4 mm. diameter 14.8 mm.
Figs. 59. 62. Natica marochiensis Gmelin. UCLA cat. no. 48375: loc. no. 1388 CIT; (59)

apertural view. (62) apical view, x 1; height 16.9 mm; diameter 14.6 mm.
Figs. 60. 63. Cymatium gracile ? (Reeve). UCLA cat. no. 48376; loc. no. 1388 CIT; (60)

apertural view. (63) abapertural view. x2; height 19.4 mm; diameter 13.7 mm.
Fig. 61. Cymatium baycri Altena. CAS cat. no. 53513: loc. no. 3x RED; apertural view.

x2; height 25.3 mm; diameter 13.5 mm.
Fig. 64. Distorsio reticulata (Roding). UCB cat. no. 10877; loc. no. 1 Ix RED: abapertural

view. X 1; height 32.5 mm: diameter 22.5 mm.
Fig. 65. Phalium glauca (Linnaeus). UCB cat. no. 10878; loc. no. llx RED: partial

exterior of last whorl, x 1.
Fig. 66. Apollon bitubercularis (Lamarck). UCB cat. no. 10879; loc. no. llx RED; aper-
tural view. X 1: height 33.5 mm: diameter 20.0 mm.
Fig. 67. Murcx sobrimis (A. Adams). UCB cat. no. 10880; loc. no. llx RED: apertural

view. X 1; height 26.0 mm; diameter 20.5 mm.
Fig. 68. Bursa rami ? (Linnaeus). UCLA cat. no. 48377; loc. no. 1388 CIT; apertural

view. X 1; height 32.0 mm: diameter 22.6 mm.

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48 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

Plate 6

Figs. 69. 70. Mehmgena gigas (Martin). CAS cat. no. 2387: loc. no. 5x RED: (69) aper-
tural. and (70) apical views, x 1: height 101 mm; diameter 86.4 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

50 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

Plate 7

Figs. 71. 72. Paramtiaria phiUppinariim (Reeve). UCLA cat. no. 48378: loc. no. 1388

CIT: (71) apertural. and (72) abapertiiral views. \2: height 20.5 mm: diameter 10.2

mm.
Fig. 73. Melongena galeodes (Lamarck). CAS cat. no. 53.'i32: loc. no. 2\ RED: apertural

view. X 1; height 44.6 mm: diameter 34.6 mm.
Fig. 74. Hindsia acuminata (Reeve). UCB cat. no. 10881: loc. no. 11\ RED: apertural

view. X 1: height 30.7 mm: diameter 17.3 mm.
Figs. 75, 79. Arcularia cf.A. globosa (Quoy and Gaimard). CAS cat. no. 53533: loc. no.

2.\ RED: (75) abaperturaL and (79) apertural views, x2: height 1 1.7 mm: diameter 7.8

mm.
Fig. 76. Hebra siihspinosa (Lamarck). UCL.A cat. no. 483'"9: loc. no. 1388 CIT: apertural

view, x2; height 13.6 mm: diameter 8.7 mm.
Fig. 77. Ht'hrajonkeri (Martin). UCLA cat. no. 48380: loc. no. 1388 CIT: apertural view ,

x2: height 12.8 mm: diameter 8.5 mm.
Fig. 78. \iorha sp. cf. .V. gimmiilaia (Lamarck). UCLA cat. no. 48381: loc. no. 1388

CIT: apertural view. x2; height 12.9 mm: diameter 8.4 mm.
Figs, 80, 81. Arcularia rhcrsitcs (Bruguiere). UCLA cat. no. 48382: loc. no. 1388 CIT;

(80) apertural, and (81) abapertural views. x2: height 13.2 mm: diameter 9.3 mm.
Figs. 82. 83. Arcularia bimaculosa (A. Adams). UCLA cat. no. 48383: loc. no. 1388 CIT:

(82) apertural. and (83) abapertural views. x3; height 9.9 mm: diameter 7.2 mm.
Fig. 84. Arcularia sp. {3. =?A. globosa (Quoy and Gaimard). C.-\S cat. no. 53534: loc.

no. 2x RED; abapertural view, x3; height 10.0 mm; diameter 7.9 mm.
Fig. 85. Arcularia sp. a. CAS cat. no. 53514: loc. no. 3.\ RED: abapertural view. x3:

height 10.2 mm; diameter 6.7 mm.
Figs. 86, 87. Clu'lanassa elcgantissima Shuto 1969. CAS cat. no. 535 15: loc. no. 3.\ RED;

(86) apertural, and (87) abapertural views, x2: height 16.5 mm; diameter 9,5 mm.

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52 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 8

Fig. 88. Alectrlon sp. qL A. coronatus (Lamarck). UCLA cat. no. 48384; loc. no. 1388

CIT; apertural view, x2; height 21.0 mm; diameter 12.7 mm.
Fig. 89. Alectrion verbeeki (Martin). CAS cat. no. 53542; loc. no. 4x RED; apertural

view. x2; height 18.5 mm; diameter 9.1 mm.
Fig. 90. Alectrion dispar (A. Adams). CAS cat. no. 53516; loc. no. 3x RED; apertural

view. x2; height 17.1 mm; diameter 10.5 mm.
Figs. 91. 95. Alectrion sinusigera ? (A. Adams). UCLA cat. no. 48385; loc. no. 1388

CIT; (91) apertural, and (95) abapertural view, x3; height 1 1.2 mm; diameter 6.4 mm.
Fig. 92. Alectrion cf. A. succinctus (A. Adams). UCLA cat. no. 48386; loc. no. 1388

CIT; apertural view. x3; height 13.7 mm; diameter 7.6 mm.
Figs. 93, 94. Alectrion sordida ? (A. Adams). =1 A. coronatus (Lamarck). CAS cat. no.

53542; loc. no. 4x RED; (93) apertural, and (94) abapertural view, x3; height 10.4 mm;

diameter 5.4 mm.
Fig. 96. Alectrion guudiosus (Hinds). UCLA cat. no. 48387; loc. no. 1390 CIT; apertural

view, x2; height 18.8 mm; diameter 9.3 mm.
Fig. 97. Alectrion crenidatus (Lamarck). UCLA cat. no. 48388; loc. no. 1388 CIT; aper-
tural view, x2; height 20.6 mm; diameter 11.8 mm.
Fig. 98. Alectrion canalicnlatus (Lamarck). CAS cat. no. 53517; loc. no. 3x RED; aper-
tural view, X 1; height 27.3 mm; diameter 1 1.0 mm.
Fig. 99. Alectrion cdgidus (Reeve). UCLA cat. no. 48389; loc. no. 1388 CIT; apertural

view, x2; height 17.3 mm; diameter 10.0 mm.
Fig. 100. Alectrion euglyptus (Sowerby). CAS cat. no. 53543; locality 4x RED; apertural

view, x2; height 20.5 mm; diameter 1 1.3 mm.
Fig. 101. Oliva reticulata (R5ding). UCB cat. no. 10882; loc. no. llx RED; abapertural

view, X I; height 33.0 mm; diameter 13.7 mm.
Fig. 102. Oliva oliva Linnaeus. CAS cat. no. 53518; loc. no. 3x RED; apertural view.

x3; height 1 1.0 mm; diameter 6.4 mm.
Fig. 103. Oliva funebralis Lamarck. UCB cat. no. 10883; loc. no. llx RED; apertural

view, x I; height 38.9 mm; diameter 18.9 mm.

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54 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 9

Fig. 104. Mitni fidiietnim Reeve. UCLA cat. no. 48390: loc. no. 1388 CIT: apertural
view. x2; height 19.4 mm: diameter 7.2 mm.

Fig. 105. Mitra intcrliratu Reeve. UCLA cat. no. 48391: loc. no. 1388 CIT: apertural
view. x3: height 14.3 mm: diameter 5.3 mm.

Fig. 106. Vexillum subdivisum (Gmelin). UCLA cat. no. 48392: loc. no. 1388 CIT: aper-
tural view. X 1: height 48.4 mm: diameter 16.5 mm.

Fig. 107. Vexillum ainanda (Reeve). CAS cat. no. 53519: loc. no. 3x RED: apertural
view. x2: height 22.3 mm: diameter 7.6 mm.

Fig. 108. Vexillum obeliscus (Reeve). UCB cat. no. 10884: loc. no. llx RED: apertural
view. X 1; height 28.9 mm: diameter 10.0 mm.

Fig. 109. Vexillum cruentatum (Gmelin). UCLA cat. no. 48393: loc. no. 1388 CIT: aper-
tural view. x3: height 15.5 mm: diameter 5.9 mm.

Fig. 110. Vexillum formosense (Sowerby). UCLA cat. no. 48394: loc. no. 1388 CIT:
apertural view. x2: height 22.0 mm: diameter 9.6 mm.

Fig. 111. Vexillum gembacanum ? (Martin). CAS cat. no. 53520: loc. no. 3x RED: aper-
tural view. x2: height 22.8 mm: diameter 10.6 mm.

Fig. 1 12. Vexillum sp. cf. V. amanda (Reeve). UCLA cat. no. 48395: loc. no. 1390 CIT:
apertural view. x2; height 26.4 mm: diameter 10.2 mm.

Fig. 1 13. Vexillum costellaris (Lamarck). UCLA cat. no. 48396: loc. no. 1388 CIT: aper-
tural view, x 1: height 34.3 mm: diameter 14.0 mm.

Fig. 114. Vexillum vulpecula (Linnaeus). CAS cat. no. 53521: loc. no. 3x RED: apertural
view. X 1: height 39.2 mm: diameter 13.3 mm.

Fig. 115. Pterygia sinensis (Reeve). UCB cat. no. 10885: loc. no. llx RED: apertural
view. x2: height 23.8 mm: diameter 9.5 mm.

Fig. 116. Trigonostoma crenifera (Sowerby). UCLA cat. no. 48397: loc. no. 1388 CIT:
apertural view. x2: height 12.0 mm: diameter 9.8 mm.

Fig. 1 17. Cancellaria verbeeki Martin. UCLA cat. no. 48398: loc. no. 1388 CIT: apertural
view. x2: height 22.8 mm: diameter 14.0 mm.

Fig. 118. Cancellaria asperella (Lamarck). UCB cat. no. 10886: loc. no. llx RED; aba-
pertural view of last whorl. x2: height 17.5 mm: diameter 14.8 mm.

Fig. 1 19. Harpa conoidalis Lamarck. UCB cat. no. 10887: loc. no. 1 Ix RED: abapertural
view. X 1: height 45.6 mm: diameter 28.0 mm.

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56 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES. No. 129

Plate 10

Fig. 120. Marginclla katikalcnsis ? Cossmann. CAS cat. no. 53544: loc. no. 4x RED:

apertural \ie\\. x2: height 16.0 mm: diameter 8.5 mm.
Fig. 121. Tunis nodiliratus Smith. CAS cat. no. 53522: loc. no. 3\ RED: apertural \ie\v.

x2: height 20.2 mm: diameter 12.2 mm.
Fig. 122. Tunis crispa Lamarck. CAS cat. no. 53535: loc. no. 2\ RED: abapertural \ie\\ .

X 1: height 30.5 mm; diameter 13.5 mm.
Fig. 123. Lopliiotonui "mannorata" (Lamarck). UCB cat. no. 10888: loc. no. ll.x RED:

apertural view, x 1: height 42.2 mm: diameter 1 1.5 mm.
Fig. 124. Lophiotoma gcndingancnsis (Martin). CAS cat. no. 53545: loc. no. 4.\ RED:

apertural view. x2: height 27.0 mm: diameter 10.0 mm.
Fig. 125. Lophiotoma acuta ? (Perry). CAS cat. no. 53523: loc. no. 3x RED: apertural

view. x2: height 29.0 mm: diameter 10.5 mm.
Fig. 126. Turricula losariensis ? (Martin). CAS cat. no. 53524: loc. no. 3\ RED: apertural

view. x2: height 21.9 mm: diameter 7.4 mm.
Fig. 127. Cnissispira pscudoprincipalis (Yokoyama). UCB cat. no. 10889: loc. no. llx

RED: apertural view. x2: height 20.7 mm: diameter 7.0 mm.
Fig. 128. Crassispira sp. cf. C. Imtaii MacNeil. UCB cat. no. 10890: loc. no. 1 1\ RED:

apertural view. x2: height 26.7 mm: diameter 8.3 mm.
Fig. 129. Compsodrillia torvita MacNeil. CAS cat. no. 53525: loc. no. 3\ RED: apertural

view. x3: height 22.4 mm: diameter 8.0 mm.
Fig. 130. Eucithara funiculata (Reeve). UCL.A cat. no. 48399: loc. no. 1388 CIT: aper-
tural \iew. x3: height 16.4 mm: diameter 11.6 mm.
Fig. 131. Inquisitor ncglectus ? (Martin). CAS cat. no. 53536: loc. no. 2x RED: abaper-
tural view. x2: height 26.9 mm: diameter 9.4 mm.
Fig. 132. Gemmula speciosa (Reeve). CAS cat. no. 53526: loc. no. 3.\ RED: apertural

view, x 1: height 39.1 mm: diameter 16.4 mm.
Fig. 133. Gemmula monilifcra (Pease). CAS cat. no. 53549: loc. no. 3\ RED: apertural

view. x3: height 18.2 mm; diameter 11.2 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

, 124

129

P %p

132 fr

^y 133

58 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 1 1

Figs. 134, 138. Conns socialis Martin. UCB cat. no. 10891; loc. no. llx RED; (134)
apertural. and (138) apical view, x 1; height 39.6 mm; diameter 19.0 mm.

Figs. 135. 139. Conns kiencri Reeve. UCB cat. no. 10892; loc. no. llx RED; (135) aper-
tural. and (139) apical view, xl; height 31.3 mm; diameter 15.1 mm.

Figs. 136. 140. Conns ngavianus Martin. CAS cat. no. 53546; loc. no. 4x RED; (136)
apertural. and (140) apical view, x 1; height 35.7 mm; diameter 19.8 mm.

Figs. 137. 141. Conns tcssnlatiis Born. UCB cat. no. 10893; loc. no. llx RED; (137)
apertural. and (141) apical views. x2; height 20.2 mm; diameter 10.8 mm.

Fig. 142. Conns fignllnns Linnaeus = C. loroisii Kiener. UCLA cat. no. 48400; loc. no.
1389 CIT; apertural view, x 1; height 28.2 mm; diameter 21.3 mm.

Fig. 143. Conns longnrionis Kiener. UCB cat. no. 10894; loc. no. llx RED; abapertural
view. x3; height 17.1 mm; diameter 6.9 mm.

Fig. 144. Conns mcnengtenganns Martin. CAS cat. no. 53537; loc. no. 2x RED; aba-
pertural view. X 1; height 67.6 mm; diameter 18.7 mm.

Fig. 145. Conns inscnlptus Kiener. UCB cat. no. 10895; loc. no. llx RED; abapertural
view. x2; height 18.8 mm; diameter 8.3 mm.

Fig. 146. Terebra pamotanensis Martin. CAS cat. no. 53547; loc. no. 4x RED; apertural
view, x2; height 25.6 mm; diameter 8.4 mm.

Fig. 147. Terebra dnpUcata ? Linnaeus. UCLA cat. no. 48401; loc. no. 1389 CIT; aper-
tural view, x 1; height 43.8 mm; diameter 10.9 mm.

Fig. 148. Terebra mynriformis ? Fischer. UCB cat. no. 10896; loc. no. 1 Ix RED; apertural
view, xl; height 34.3 mm; diameter 10.6 mm.

Fig. 149. Pyramidella sp. CAS cat. no. 53548; loc. no. 4x RED; apertural view. x2;
height 10.9 mm; diameter 7.0 mm.

Fig. 150. Pnpa sulcata (Gmelin). CAS cat. no. 53538; loc. no. 2x RED; apertural view,
xl; height 18.8 mm; diameter 11.4 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

134

135

^^ 136

138

139

/*i-2k

140

tz:

"^ 143

145

144

146

150

60 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 12

Figs. 151-153. Yoldia sp. f3. UCLA cat. no. 48402; loc. no. 1388 CIT: (151) exterior left

valve. (152) dorsal view of both valves. (153) exterior right valve. x2: height 9.4 mm:

length 16.6 mm.
Fig. 154. Anadara pangkaensis (Martin). CAS cat. no. 53527: loc. no. 3x RED: exterior

left valve, x 1: height 27.0 mm: length 37.4 mm.
Fig. 155. Anadara antiquata (Linnaeus). UCLA cat. no. 48403: locality no. 1388 CIT:

exterior left valve, x 1; height 28.2 mm; length 39.0 mm.
Fig. 156. Anadara biformis (Martin). UCLA cat. no. 48404: loc. no. 1390 CIT; exterior

of right valve, x 1; height 33.5 mm; length 47.5 mm.
Fig. 157-159. Anadara granosa (Linnaeus). UCLA cat. no. 48405; loc. no. 1452 CIT.

Santa Barbara. Panay: (157) exterior left valve; (158) interior left valve: (159) dorsal

view both valves, x 1; height 39.4 mm: length 53.5 mm; thickness of both valves 37.8

mm.
Fig. 160-161. Anadara cornea (Reeve). UCLA cat. no. 48406; loc. no. 1388 CIT; (160)

exterior right valve; (161) exterior left valve, both x 1; height, right valve. 30.2 mm;

length, right valve, 33.7 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

''"iiW

'Him

155

il s

\\\

159

160

161

62 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. IZ'J

Plate 13

Fig. 162. Anadara sp. a. CAS cat. no. 53528; loc. no. 3x RED: exterior left valve. x2;

height 17.3 mm; length 23.0 mm.
Fig. 163. Trisidos semitorta (Lamarck). UCLA cat. no. 48417; loc. no. 1454. Bagacay.

Panay; exterior left valve, x 1; height 33.0 mm; length 48.0 mm.
Figs. 164. 165. Striarca olivacea (Reeve). UCLA cat. no. 48407; loc. no. 1388 CIT; (164)

exterior, and ( 165) interior of left valve. x2; height 7.9 mm; length 1 1.7 mm.
Fig. 166. Striarca sinensis Habe & Kosuge. non Thiele. UCLA cat. no. 48408; loc. no.

1390 CIT; exterior of right valve. x2; height 13.0 mm; length 18.2 mm.
Figs. 167. 168. Limopsis sp. ^8. UCB cat. no. 10897; loc. no. llx RED; (167) exterior,

and (168) interior of left valve. x3; height 11.9 mm; length 11.6 mm.
Fig. 169. Glycymeris sp. a. UCB cat. no. 10898; loc. no. 1 Ix RED; exterior left (?) valve.

X 3; height 10.9 mm; length 1 1 .0 mm.
Fig. 170. Glycymeris sp. B. UCB cat. no. 10899; loc. no. llx RED; exterior of right

valve. X 1; height 36.0 mm; length 38.6 mm.
Fig. 171. Glycymeris sp. A. UCB cat. no. 10900; loc. no. llx RED; exterior of right

valve. X 1; height 37.3 mm; length 38.2 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

164

■'■S^r |g^

167

170

169

'^^ III WW

171

64 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 14

Fig. 172. Amiissium pleuroncctes ? (Linnaeus). UCLA cat. no. 48409: loc. no. L^90 CIT;

exterior of left valve, x 1; height 30.5 mm; length 29.3 mm.
Fig. 173. Chlamys crassicostatus ? (Sowerby). UCB cat. no. 10901; loc. no. llx RED;

exterior of right valve. x2; height 17.5 mm; length 15.4 mm.
Figs. 174-176. Cycladicama oblonga (Sowerby). UCLA cat. no. 48410; loc. no. 1390

CIT; (174) exterior of right valve. (175) anterior view, both valves, (176) dorsal view

both valves, x 1; height 30.3 mm; length 34.5 mm; thickness of both valves 20.8 mm.
Figs. 177, 180. Cardita canalicidata Reeve. UCB cat. no. 10902; loc. no. 1 Ix RED; ( 177)

exterior of right valve. (180) exterior of left valve. x2; height of right valve. 14.4 mm;

length of right valve. 17.9 mm.
Fig. 178. LaevkanUiim cf. L. midtipunctatiim (Sowerby). UCB cat. no. 10903; loc. no.

1 Ix RED; exterior of right valve, x 1; height 37.0 mm; length 29.5 mm.
Fig. 179. Laevicardium imicolor ? (Sowerby). UCB cat. no. 10904; loc. no. llx RED;

exterior of left valve, x2; height 30.8 mm; length 21.1 mm.
Figs. 181, 182. Hemidonax donacaeifonnis (Spengler). UCLA cat. no. 48411; loc. no.

1388 CIT; (181) exterior, and (182) interior of left valve, x2; height 14.6 mm; length

18.8 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

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66 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 15

Fig. 183. Meiocardia aff. M. vulgaris (Reeve). UCB cat. no. 10905: loc. no. llx RED:

exterior of left valve, x 1: height 33.0 mm: length 47.3 mm.
Fig. 184. Callista erycina (Linnaeus). UCB cat. no. 10906: loc. no. llx RED: exterior

of right valve, xl: height 33.2 mm: length 48.3 mm.
Fig. 185. Cyclina sinensis ? (Gmelin). UCLA cat. no. 4(S412: loc. no. 1389 CIT: exterior

of left valve, x 1: height 44.0 mm: length 47.0 mm.
Fig. 186. dementia pupyracea Gray. UCLA cat. no. 48413: loc. no. 1390 CIT: exterior

of right valve. x2: height 19.4 mm: length 26.5 mm.
Fig. 187. Paphia eiiglypta (Philippi). UCLA cat. no. 48414: loc. no. 1390 CIT: exterior

of right valve, x 1; height 20.5 mm: length 35.0 mm.
Fig. 188. Paphia sp. a. UCB cat. no. 10907: loc. no. llx RED: exterior of left valve.

X 1: height 22.6 mm: length 33.8 mm.
Fig. 189. Plucamen isabellina (Philippi). UCB cat. no. 10908: locality 1 Ix RED: exterior

of left val\e. x 1: height 31.8 mm: length 35.2 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

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187

68 OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 16

Figs. 190-192. Corbula fortisiikata Smith. UCLA cat. no. 48415: loc. no. 1388 CIT;

(190) right exterior. (191) both valves, dorsal view. (192) left exterior. x2; height 12.4

mm: length 15.4 mm: thickness both valves 10.8 mm.
Figs. 193-195. Corbula lamellata Fischer. CAS cat. no. 53539: locality 2x RED: (193)

right exterior. (194) dorsal view of both valves. (195) left exterior. x2; height 11.3

mm: length 16.6 mm: thickness both valves 8.8 mm.
Figs. 196-198. Corbula "scaphoides" Tesch. non Hinds. UCLA cat. no. 48416: loc. no.

1388 CIT: (196) left exterior. (197) right exterior, and (198) dorsal view of both valves.

x2: height 14.1 mm: length 19.4 mm: thickness of both valves 11.6 mm.
Fig. 199. Corbula sp. UCB cat. no. 10909: loc. no. llx RED: exterior of right valve.

x2: height 16.5 mm: length 21.6 mm.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

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196

197

OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 17

Fig. 200. "Actaeon retkulatus K. Martin": Dickerson 1922. pi. 2. fig. 2. = Pupa sul-
cata (Gmelin). fig. 150. this paper.

Fig. 201. Actaeon reticulatus nov. spec: Martin 1883-1887, pi. IV. fig. 42 (original fig-
ure).

Fig. 202. Conus omatissimus Martin: Martin 1891-1906. p. 12, pi. I. fig. 8.

Fig. 203. "Conus omatissimus K. Martin": Dickerson 1922. pi. 2. fig. 11; = Conus
socialis Martin, this paper.

Fig. 204. "Conus hardi K. Martin": Dickerson 1922. pi. 2. fig. 15. = Conus loroisii
Kiener, fig. 142. this paper.

Fig. 209. Conus hardi Martin: Martin 1891-1906, p. 18. pi. III. fig. 38.

Fig. 205. Terebra bicincta nov. spec: Martin 1879-80. p. 33. pi. VI. fig. 13b (original
figure). Not found in present study.

Fig. 206. "Terebra bicincta K. Martin": Dickerson 1922. pi. 5. fig. 14.

Fig. 207. "Terebra Javana K. Martin.": Dickerson 1922, pi. 5, fig. 15. Not found in
present study.

Fig. 208. Terebra javana nov. spec: Martin 1879-80, p. 32. pi. VI. fig. 11 (original

figure).

Fig. 210. "Mitra javana K. Martin": Dickerson 1922. pi. 3. fig. 3a. =Vexillum vulpecula
(Linnaeus), fig. 114. this paper.

Fig. 211. Mitra javana nov. spec: Martin 1879-80, p. 27. pi. VI. fig. 2 (original figure).

Fig. 212. "Mitra bucciniformis K. Martin": Dickerson 1922. pi. 3. fig. 5, =VexHlum
cruentatum (Gmelin), fig. 109. this paper.

Fig. 213. Mitra bucciniformis nov. spec: Martin 1879-1880. p. 28. pi. VI. fig. 4a (orig-
inal figure).

Fig. 214. "Mitra junghuhni (?) K. Martin": Dickerson 1922. pi. 3, fig. 4, =Mitra inter-
lirata Reeve, fig. 105, this paper.

Fig. 215. Mitra junghuhni Martin: Tesch 1915. p. 44. pi. LXXIX(7), fig. 94b.

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

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OCCASIONAL PAPERS OF THE CALIFORNIA ACADEMY OF SCIENCES, No. 129

Plate 18
Fig. 216. •■Marginella simplicissima K. Martin": Dickerson 1922. pi. 3. fig. lib.

=Marginella sp., this paper.
Fig. 217. Marginella simplicissima nov. spec: Martin 1879-80. p. 24. pi. V. fig. 3

(original figure).
Fig. 218. •■Columhclla bandongensis K. Martin"": Dickerson 1922. pi. 2. fig. 16.

= Parametaria philippinarum (Reeve), fig. 71-72. this paper.
Fig. 219. Columbdla bamiongensis Martin: Martin 1891-1906. p. 118. pi. XVIII. fig.

263.
Fig. 220. ■■Ccrithium jenkinsi K. Martin"": Dickerson 1922. pi. 2. fig. 7. =Ccrithidea

jcnkinsi (Martin), fig. 18. this paper.
Fig. 221. Cerithiiim jenkinsi nov. spec: Martin 1879-80. p. 65 pi. XI. fig. 6 (original

figure). =C. cingidata (Gmelin). Van Regteren Altena 1942. vol. 12. p. 7.
Fig. 222. ■■Cerithiiim bandongensis K. Martin"": Dickerson 1922. pi. 2. fig. 6. This

species not found in present study.
Fig. 223. Cerithiiim bandongense nov. spec: Martin 1879-1880. p. 63. pi. XI. fig. 5a

(original figure).
Fig. 224. •■Corbiila socialis K. Martin": Dickerson 1922. pi. 6. fig. 11. Not found in

present study.
Fig. 225. Corbiila socialis nov. spec: Martin 1879-80. p. 92. pi. XV. fig. 10a (original

figure).
Fig. 226. ■•Cerithiiim herklotsi K. Martin"": Dickerson 1922. pi. 2. fig. 9a. =Cerithiiim

jonkeri Martin, this paper.
Fig. 227. Potamides herklotsi (Martin): Martin 1921. p. 473. pi. (Ill) LX. fig. 76.
Fig. 228. ■■Strombiis cWfiisiis K. Martin"": Dickerson 1922. pi. 5. fig. 8. Not found in

present study.
Fig. 229. Fiisns verbeeki spec, nov.: Martin 1891-1906. p. 85. pi. XIII. fig. 195.

^■? Strombiis CD fnsiis spec nov.. Martin 1879-80. p. 50, pi. IX. fig. 9 (original

figure).

POPENOE & KLEINPELL: VIGO FORMATION AND ITS FAUNA

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